Characterisation of badlands and modelling of soil erosion in the Isábena watershed, NE Spain Charakterisierung und Modellierung von Bodenerosion auf Badlands im Isábena-Einzugsgebiet, NO-Spanien Diplomarbeit von: Katharina Joana Appel Vorgelegt bei: Prof. Dr. Christian Opp Lehrstuhl für Hydrologie und Bodenkunde am Fachbereich Geographie der Universität Marburg Dr. Eva Nora Müller am Institut für Geoökologie der Universität Potsdam Oktober, 2006
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Characterisation of badlands and modelling of soil erosion in the Isábena watershed, NE
Spain
Charakterisierung und Modellierung von Bodenerosion auf Badlands im Isábena-Einzugsgebiet, NO-Spanien
Diplomarbeit
von: Katharina Joana Appel
Vorgelegt bei:
Prof. Dr. Christian Opp
Lehrstuhl für Hydrologie und Bodenkunde am Fachbereich Geographie der Universität Marburg
Dr. Eva Nora Müller am Institut für Geoökologie der Universität Potsdam
Oktober, 2006
2
Abstract Badlands are hillslopes of unconsolidated sediments with no or little vegetation that cannot be
used for agriculture and are characterized by their desert like appearance and their very high
soil erosion rates. This study assesses the feasibility of modelling soil erosion rates from
badlands of the Isabena Watershed in the Pre-Pyrenees, NE Spain using a field-work
integrated, process-based, semi-distributed modelling approach. For this purpose, a field
campaign was carried out to collect key geomorphological and soil hydraulic data for model
parameterization. Four typical badland formations were selected in the field as a function of
form, extent and internal gully system to enable a comparative study of badland processes.
The four badland types were then modelled using a soil-erosion routine based on the MUSLE
(Modified Universal Soil Loss Equation) approach coupled with the hydrological model
WASA. Altogether, three spatial discretizations of increasing complexity were applied.
The fieldwork results as well as the modelling results and a sensitivity analysis are presented
and discussed. The model version applied in this study is attached on a CD.
Zusammenfassung Badlands sind kahle Hänge aus Lockermaterial die extrem hohe Erosionsraten aufweisen.
Diese Arbeit befasst sich mit der Modellierung von Erosionsraten auf Badland-Hängen im
Isábena – Einzugsgebiet, einem Teileinzugsgebiet des Ebrobeckens, in Nordost - Spanien. Bei
dem angewandten Model WASA (Water Availability in Semi-arid Areas) handelt es sich um
ein räumlich verteiltes, prozessorientiertes hydrologisches Model welches mit der Modified
Universal Soil Loss Equation (MUSLE) kombiniert wurde um ereignisbezogene
Erosionsraten zu errechnen. Die Parametrisierung des Modells beruht auf einer Erhebung
relevanter Parameter wie Form, Größe, Exposition, Hangneigung, Vegetationsbedeckung,
Infiltrabilität und Korngrößenverteilung des Oberbodens, die in vier exemplarischen Badlands
im Untersuchungsgebiet durchgeführt wurde. Weitere Parameter wurden anhand von Werten
aus der Literatur ergänzt. Insgesamt wurden drei räumliche Diskretisierungen
unterschiedlicher Komplexität angewendet. Des Weiteren wurde eine Sensitivitätsanalyse
durchgeführt. Die Validierung der Modelergebnisse basiert auf Werten aus der Literatur in
Ermangelung von Messdaten aus dem Untersuchungsgebiet. Durchführung und Ergebnisse
der Feldarbeit sowie der Modellierung werden in der Arbeit vorgestellt und diskutiert. Die
Version des Modells die für diese Studie angewendet wurde ist in digitaler Form auf einer CD
beigefügt.
3
Acknowledgement I would like to thank Dr. Eva Nora Müller, who guided me through this work and introduced me to environmental modelling, for all the help and support I received during this last year. I would also like to thank Prof. Dr. Christian Opp for his critical comments and uncomplicated support. My gratitude goes to all the other members of the SESAM-Project, especially Till Francke for his patience in answering my questions. Many thanks to my friends Katrin Friedrich and Henrik von Wehrden for proofreading this work. And finally, I would like to thank my family for always supporting my decisions.
4
1. Introduction 8
2. Characterization of Badlands – a literature review 10
2.1. Definition and characteristics 10
2.1.1. Arid badlands 10
2.1.2. Semi-arid badlands 10
2.1.3. Humid badlands 11
2.2. Erosion processes 11
3. Study area 14
3.1. Localization 14
3.2. Climate 15
3.3. Hydrology 16
3.4. Geology and geomorphology 17
3.5. Soils 17
3.6. Vegetation and land use 18
3.7. Socioeconomic aspects 18
4. Methodology 19
4.1. Introduction to the modelling concepts 19
4.1.1. Introduction to the WASA-Model 19
4.1.2. Process representation 22 4.1.2.1. Interception model 22 4.1.2.2. Evapotranspiration model 22 4.1.2.3. Infiltration model 24 4.1.2.4. Soil water model 26 4.1.2.5. Lateral distribution of surface and subsurface flow between soil
vegetation components 26 4.1.2.6. Lateral distribution between TCs of surface and subsurface runoff 27
4.1.3. The Modified Universal Soil Loss Equation 29 4.1.3.1. Introduction to the Modified Universal Soil Loss Equation 29 4.1.3.2. Lateral distribution of sediment 32
4.2.2. Detail study 38 4.2.2.1. Description 38 4.2.2.2. Results 43
5
4.3. Parameterization of the WASA-Model 45
4.3.1. Spatial discretization 1 – the sensitivity analysis 45
4.3.2. Spatial discretization 2 and 3 46
4.3.3. Derivation of soil types and their hydraulic properties 49
4.3.4. Derivation of vegetation types and their hydraulic properties 50
4.3.5. Derivation of climate data 51
4.4. Summary 52
5. Results and discussion 53
5.1. Results of spatial discretization 1 53
5.1.1. Hydrological parameters 54
5.1.2. MUSLE Parameters 55
5.2. Results for spatial discretization 2 58
5.2.1. Results at the level of terrain components 58 5.2.1.1. Runoff generation at the level of terrain components 58 5.2.1.2. Sediment generation at the level of terrain components 59
5.2.2. Results at the level of subbasins 63 5.2.2.1. Runoff generation at the level of subbasins 63 5.2.2.2. Sediment generation at the level of subbasins 64
5.3. Results of spatial discretization 3 67
5.3.1. Runoff generation for spatial discretization 3 67
5.3.2. Sediment production for spatial discretization 3 at the level of terrain components 68
5.3.3. Sediment production for spatial discretization 3 at the level of subbasins 69
5.4. Validation of the model 71
6. Summary and conclusion 73
7. References 75
8. Appendix 81
8.1. Appendix 1: Results of pH measurements and electric conductivity measurements for the soil samples taken within the detail study 81
8.2. Appendix 2: vegetation parameters needed for parameterization of the WASA module 82
8.3. Appendix 3: Poster about the sensitivity analysis conducted. Presented at the European Geosciences Union General Assembley 2006 in Vienna 83
6
Tabels
Table 4-1: Routing and transport modes for sediment applied during this study ---------------------------34
Table 4-2: Main characteristics of the four Badlands --------------------------------------------------------------37
Table 4-3: Saturated hydraulic conductivity measured on badland slopes and derived by pedotransfer functions applying the ROSETTA model (Shaap, 2000). Sample ID is composed of the measurement number and the depth in which it was conducted. 0 = on natural soil surface, 30 = 30 cm below soil surface.------------------------------------------------------------------------------------------------------------------------40
Table 4-4: Results of chemical soil analysis -------------------------------------------------------------------------44
Table 4-5: Range of values as used for the sensitivity analysis-------------------------------------------------46
Table 4-6: Spatial discretization 2 for the four badlands ----------------------------------------------------------48
Table 4-7: Soil parameters required by the WASA model --------------------------------------------------------49
Table 4-8: Landcover classes used for parameterization in WASA and the corresponding classes of the PlaPaDa -----------------------------------------------------------------------------------------------------------------50
Table 4-9: Model input parameters for vegetation------------------------------------------------------------------51
Table 5-1: Mean annual runoff [m³/a] per TC ------------------------------------------------------------------------58
Table 5-2: Mean annual runoff yield [m³/m³a] per TC--------------------------------------------------------------58
Table 5-3: Size of each TC in m² ---------------------------------------------------------------------------------------59
Table 5-4: Slope length of terrain component in m-----------------------------------------------------------------59
Table 5-5: Mean annual sediment production [t/a] for the four badlands at the level of terrain components ------------------------------------------------------------------------------------------------------------------61
Table 5-6: Mean annual sediment yield [t/m²a] per TC and routing mode------------------------------------62
Table 5-7: Portion rill erosion of the sediment production of one TC ------------------------------------------62
Table 5-8: Runoff, runoff yield and discharge coefficient at the level of BL ----------------------------------63
Table 5-9: Sediment concentration in [g/l] at the level of BL for the four routing and transport modes63
Table 5-10: Mean annual sediment production [t/a] for each BL------------------------------------------------64
Table 5-11: Mean annual sediment yield [t/m²a] for each BL ----------------------------------------------------65
Table 5-12: Portion rill erosion of the sediment production of each BL----------------------------------------65
Table 5-13: Annual erosion rates in [t] of the four badlands for the years 1997 to 2005 modelled with the time series from the climate station of Pont de Suert ---------------------------------------------------------66
Table 5-14: Mean annual runoff [m³/a] at the level of terrain components and at the level of subbasin for spatial discretization 3-------------------------------------------------------------------------------------------------67
Table 5-15: Mean annual sediment production [t/a] per TC for spatial discretization 3 -------------------68
Table 5-16: Mean annual sediment yield [t/m²a] for the four BL with TC2 divided into two equal TCs 68
Table 5-17: difference in sediment production on TC2 for spatial discretization 2 and the sum of sediment production on TC2 and TC3 of spatial discretization 3 in %. Sediment production of TC2, spatial discretization 2 = 100%------------------------------------------------------------------------------------------69
Table 5-18: Mean annual sediment production [t/a] at the level of subbasins for spatial discretization 3----------------------------------------------------------------------------------------------------------------------------------69
Table 5-19: Differences in mean annual sediment production at the level of subbasin between spatial discretization 2 and 3 in %. Mean annual sediment production of spatial discretization 2 is set 100%70
Table 5-20: Comparison of results with data from literature (if not indicated, results in [t/ha a]) --------72
7
Figures
Figure 2-1 a and b: Coarse material in the channel of a badland probably deriving from mass movements-------------------------------------------------------------------------------------------------------------------13
Figure 3-1: Location of the Isábena cacthment whithin the Ebro basin; yellow area = Ebro basin; red area = Isábena catchment------------------------------------------------------------------------------------------------14
Figure 3-2: Location of the Isábena catchment within the catchment of the Barasona reservoir and of the Villacarli sub catchment within the Isábena catchment-------------------------------------------------------14
Figure 4-1: Hierarchical multi-scale disaggregation scheme for structuring river basins into modelling units in WASAFigure taken from Güntner (2002) with permission.---------------------------------------------21
Figure 4-2: Lateral distribution of runoff between soil vegetation components on one TC. (Figure taken from Güntner (2002); with permission) --------------------------------------------------------------------------------27
Figure 4-3: Lateral transfer of water and sediment from higher to lower TC. TC = Terrain component, the number indicates the position within the landscape unit. (1= highland, 2 = slope, 3 = lowland), taken from Güntner, 2002, with permission. -------------------------------------------------------------------------28
Figure 4-4: the four catchments of the badlands used for modelling spatial discretization 3 and 3. (Aerial picture form Sept. 1982, taken by I.G.N.) -------------------------------------------------------------------35
Figure 4-5: The Villacarli sub catchment with the four study sites ----------------------------------------------35
Figure 4-6: The four study sites. In green their outer limitation, in red the main channels. Aerial fotography by I.G.N. 1982. -----------------------------------------------------------------------------------------------37
Figure 4-7: Mosses and lichens found in the forest around BL2 on a north facing slope. ----------------37
Figure 4-8: Mean slope and standard deviation of the four exemplary badlands ---------------------------38
Figure 4-9: Comparison between mean vegetation cover of slopes -------------------------------------------38
Figure 4-10: Left: Aerial photography of BL1 taken in right: Aerial photography (M.A.P.A. 2005) showing Badland 1 which has been studied in detail. Crosses mark the sample localities where the soil samples were taken during the detail study --------------------------------------------------------------------43
Figure 4-11: Mean grain size distribution for the four geomorphological units ------------------------------44
Figure 4-12: Particle size distribution of soil samples taken on badlands ------------------------------------44
Figure 5-1: Results of the sensitivity analysis for important hydraulic parameters -------------------------56
Figure 5-2:Relative runoff contribution of each TC in % ----------------------------------------------------------59
Figure 5-3: Fraction of the mean annual sediment production of every TC on four badlands for different routing modes. Routing mode A = no transfer between TCs, no transport limit; B= routing between TCs, no transport limit; C= routing between TCs, transport capacity limit according to Govers (1990) and Morgan et al. 1998 (, D=routing between TCs, transport limit maximal erosion according to the MUSLE equation. ------------------------------------------------------------------------------------------------------62
Figure 5-4: Mean annual sediment production [t/a] on each Badland for the four routing modes ------65
Figure 5-5: Event erosion rates (dots) and relative cumulative erosion (red line) on BL3 with routing mode C for climate data of the year 2000 ----------------------------------------------------------------------------66
Figure 5-6: Mean annual sediment production at the level of badlands for spatial discretization 3. Full = spatial discretization 2; stripes = spatial discretization 3----------------------------------------------------------70
8
1. Introduction Badlands are hillslopes of unconsolidated sediments. Sparse vegetation cover and steep slopes
lead to high erosion rates. In the study area, the catchment of the Barasona reservoir in NE
Spain, previous studies have identified badlands as the main sediment source (Valero-Garcés
et al. 1999). The Barasona reservoir supplies the region with drinking water, electricity and
water for irrigation purposes. The high amount of sediment input coming from the badlands
leads to a severe reduction of the storage capacity of the reservoir. Especially in dry years, the
decrease in volume leads to supply shortages and socioeconomic problems.
This study aims at gaining information on sediment production and transport rates on badland
hillslopes in order to derive erosion rates for exemplary hillslopes by means of soil erosion
modelling. For this purpose, the hydrological model WASA (Water Availability in Semi-arid
Areas) developed by Güntner (2002) was combined with the Universal Soil Loss Equation
(MUSLE) (Williams, 1975). WASA is a deterministic model composed of process-based
conceptual submodels applied to a semi distributed spatial discretization.
The erosion routine based on the MUSLE is an empirical equation that integrates over soil
erosion processes on the hillslope scale. It was developed for the estimation of soil loss on
agricultural crop land. Spatial discretization applied in WASA to account for spatial
variability of parameters is an opposed concept. Furthermore, a mathematical problem arises
due to the fact, that the area being considered is not a linear factor in the MUSLE. Its result,
sediment production, is scaled linearly from subordinated spatial units to a superordinate
spatial unit. The same accounts for slope length. Within this study, it is tested if the MUSLE
approach is able to reproduce the extreme erosion rates on the badland slopes and whether or
not it can be combined with the spatial discretization concept applied in WASA.
For parameterization of the model, two weeks of field work were conducted in order to
characterize the badlands in the study area and to measure and estimate soil hydraulic
characteristics on the badlands slopes. Parameters that could not be determined by
measurements were derived by pedotransfer functions, intersection of thematic maps in a
geographic information system or endorsed by values from literature.
Altogether, three spatial discretizations were applied: a simple one to conduct a sensitivity
analysis for estimating the range within the result would vary and to identify the importance
of relevant parameters to modelling results. The second spatial discretization applied is the
one best representing the four study sites as characterized during the field work.
The third one differs from the second one only in the number of spatial units. It was
performed to see how spatial discretization affects sediment production.
The results of these three scenarios are analyzed at different spatial levels. Since only
preliminary results of measurements of erosion rates are available for the study area,
modelling results are validated by the comparison with values from literature.
9
Recapitulating, the four objectives of this study are a) to estimate required parameterization
data from badlands in the field, b) parameterize the hydrological and soil erosion model
considering different spatial discretizations, c) carry out a sensitivity analysis and d) test and
discuss the outcome of the models.
10
2. Characterization of Badlands – a literature review
2.1. Definition and characteristics
Badlands are hillslopes of unconsolidated sediments or poorly cemented bedrock as marls,
mudstone or shales. Vegetation cover on badlands is sparse. Slopes are dissected by a dense
drainage network within v-shaped valleys (Bryan and Yair, 1982). Dominant processes
contributing to soil erosion on the hillslopes are rainsplash and overland flow as well as
piping and mass movements. Badlands are different from gullies for they include slopes and
divides (Nogueras et al. 2000) and are not only linear, discrete phenomena but can compose
whole landscapes. They usually form a mosaic of stable areas with soil and vegetation cover
and unstable, bare areas where bedrock is only covered by a thin regolith layer. Badland
development is bound to linear incision and gully erosion (Gallart et al., 2002b). The main
factor controlling badland formation is the character of the bedrock. Usually, a protective
caprock has been removed and a softer rock less resistant to erosion surfaces. Tectonics and
uplift are sometimes involved in this process but also land use changes may trigger the
formation of badlands. They are considered to be characteristic of dryland areas but they also
occur in wetter climate with high intensity storm events such as in the Mediterranean.
Gallart et al. (2002a) classify badlands according to the climate, they occur in and the
corresponding processes dominating on the hillslopes.
2.1.1. Arid badlands
Arid badlands occur in areas with about 200 mm of annual precipitation. Vegetation cover is
low due to the shortage of water. These badlands are exclusively controlled by the
characteristics of bedrock and regolith. Erosion rates are lower than expected (Wise et al.,
1982). Erosion only occurs during high intensity rainfall events, which are scarce. The slopes
are thus actually quite stable. Missing vegetation is ascribed to the low potential of seedling
survival. These landscapes are thus usually very old. The best known example for this type
are the badlands in the Northern Negev, Israel (Yair et al., 1980).
2.1.2. Semi-arid badlands
In semi-arid climate, where rainfall lies between 200 and 700 mm/a, vegetation cover on the
badlands is usually higher. Limiting factor to vegetation growth is still water availability as
suggests the asymmetric mosaic of dense vegetation cover of up to 100% on north facing
slopes and almost no plant growth on the south facing slopes due to higher insolation (Solé et
al. 1997; Cantón, 1999). Semi-arid badlands are also usually quite old and have experienced
phases of stability and instability (Calvo et al. 1991; Nogueras et al. 2000). Wise et al. (1989)
11
proved that archaeological structures had survived 4000 year on the surface of badland
landscapes in south east Spain.
Their initialisation is mostly natural. Once initiated though, they are highly susceptible to
human impact as grazing, agriculture and especially the concentration of runoff in artificial
ditches which is comparable to the creation of a gully which can easily incise in the highly
erodible regolith and soft bedrock. Examples for this type of badland can be found in
southeastern Spain and southern Italy (Bouma and Imeson, 2000; Cantón et al. 2001).
2.1.3. Humid badlands
Humid badland are found in mountainous areas as the Southern Alps (Draix, Haute Provence,
France) and the Pyrenees (Vallcebre, Catalonia and Isábena, Aragon, both in NE Spain).
Mean annual precipitation is around 700 mm or higher. Rainfall mostly occurs in form of high
intensity storm events. Vegetation growth is no longer limited by water availability but by the
high erosion rates and freezing on north exposed slopes (Regüés et al., 2002). In general,
badlands of this type are younger than the others (Clotet et al. 1988). Their formation is
triggered by mass movements that may be caused by degradation of vegetation due to human
impact. The badlands studied in this thesis belong to this type considering that mean annual
rainfall is 767 mm/a (see section 3.2). The distribution of vegetation would rather fit to the
semi-arid type though. South facing slopes within the catchment considered show a less dense
vegetation cover than the north facing slopes that carry coniferous and mixed forests (see
section 4.2.1).
2.2. Erosion processes
Parameters influencing erosion on badlands are the degree and agent of cementation of the
bedrock and particle size distribution. Soils or weathering material developing from marls,
shales or mudrock are usually rich in silt and clay but have low sand content. These
sedimentary rocks have a high porosity volume of about 10 % (Gallart et al. 2002b). The
solution of cementing agents as there are salts, sulphates or carbonates leads to enhancement
of the pores and an increase in pore volume to up to 50 %. Wetting and drying circles causing
swelling and shrinking of three-layer clays and solubilization and cristallization of salts
further destabilize the weathered bedrock and produce a layer of regolith with a characteristic
popcorn structure (Cantón et al. 2001). In areas where freezing occurs, freezing - thawing
cycles become the dominant weathering process (Gallart et al. 2000b).
Processes leading to the destruction of aggregates and particle detachment are first of all
splash erosion and slaking. Splash erosion is caused by the impact of raindrops striking the
soil surface. It increases with rainfall intensity (Cerdá, 1997). Slaking is the bursting of
aggregates occurring when aggregates wet fast and air gets trapped in the interior. Soil
resistance against these processes are related to soil cover and intrinsic characteristics as clay
12
content and content of organic matter which contribute to aggregate stability. Resistance of
regoliths against erosion on badlands is low due to the low content in organic matter (lees
than 1%). If the sodium content in the soil is high, clays become dispersive and highly
erodible. Furthermore, their dispersion leads to sealing of pores and even crusting which
reduces infiltrability and increases runoff. Cracks on the other hand enable fast infiltration at
least at the beginning of an event for they might close due to swelling if the rainfall event lasts
long enough. In areas where freezing occurs, regolith characteristics show a seasonality which
affects infiltration and runoff generation (Gallart et al, 2000a). The popcorn structure
produced in winter by freezing and thawing is destroyed and compacted over the year due to
splash erosion and slaking (Gallart et al. 2002a). The compacted soil is less permeable and
leads to higher runoff production. Runoff generation thus depends on lithology, antecedent
soil moisture conditions, duration of storms and the season.
Runoff occurs as surface runoff in rills and channels or as sheetflow but also as subsurface
runoff through pipes. Rills are nonpermanent microforms on the badland slopes and play an
important role in water and sediment conveyance.
Pipes emerge from the convergence of subsurface cracks or macropores that rapidly enlarge.
Considerable amounts of water can run through the pipes and lead to subsurface erosion.
Piping is thus a self-energizing process. The collapse of pipes is often the initialization of a
channel (Gutierrez et al., 1988). The occurrence of pipes seems to be bound to high levels of
sodium in the soil for it leads to diflocculation of clay particles which become more erodibilty
(Romero Díaz et al., 2006).
Regüés and Gallart (2004) found out, that dominant erosion processes on humid badlands
have a seasonal pattern. During winter, physical weathering produces a thin layer of regolith
of maximal 15 mm depth. During the high intensity rainfall events of spring and summer, soil
detachment and transport from the hill into the channel takes place whereas for sediment
transport within the channel into the river network longterm rainfall producing persistent
channel flow is necessary as it occurs in autumn.
Mass movements are also an important process in the formation of badlands. They are caused
by instabilization of the regolith or even bedrock and reach from smaller mudflows to larger
slumps. Huge amounts of sediment and rock are mobilized during such events (see Figure
2-1).
Badlands appear to have extremely high erosion rates. This is valid at the scale of single storm
events but mean annual rates are not necessarily high in arid to semi-arid badlands with high
interannual variability in rainfall. With increasing runoff though, erosion rates grow rapidly
(Gallart et al. 2002a). On the other hand, increasing runoff leads to more vegetation cover and
thus better protection from erosion (Nogueras et al. 2000). Cantón (1999) state that erosion
rates in humid badlands can be limited by weathering rates and the amount of disposable
sediment as show the bedrock outcrops in channels which are depleted completely almost
every year, at least in humid badlands as studied here (Clotet et al. 1988; Regüés et al 1995) (.
Event erosion rates area transport limited though (Campbell, 1989).
13
Erosion rates found in literature are highly variable due to the application of different methods
in different climates. For the humid badlands in Vallcebre, NE Spain, values between 120 t/ha
a (Gallart et al. 2005) and 550 t/ha a (Clotet Perernau et al. 1988) were recorded and ground
lowering between 7.3 and 37 mm / a (Clotet and Gallart, 1986).
Figure 2-1 a and b: Coarse material in the channel of a badland probably deriving from mass movements
14
3. Study area
3.1. Localization
The study area is a sub catchment of the Isábena watershed which is located in the Central
Pyrenees in north eastern Spain (Figure 3-1). The Isábena catchment is situated within the
autonomous community of Aragón in the province of Huesca. It is part of the Ebro basin and
extends over 445 km² which is about 0.48 % of the Ebro watershed. Mean annual runoff is 5.7
m³/s which is equivalent to 1.34 % of the total runoff of the Ebro (Verdú Arnal, 2003).
Altitude ranges between 650 m a.s.l. at its mouth and 2720 m a.s.l. at the Pico de Gallinero in
the north. The course of the Isábena river from the spring to the mouth is about 50 km long
(Gayúbar, 2000). After the confluence with the Ésera river (see Figure 3-1) a dam forms the
Barasona reservoir of 92 x 106 m3 which serves the generation of electricity, supplies
drinking water and water for irrigation purposes.
The very inhomogeneous morphology of the catchment forms various sub catchments (see
Figure 3-2), one of them being the Arroyo de Villacarli (see Figure 3-2). In this transversal
valley, the ephemeral Villacarli river carves into a layer of soft, gray marls on which badland
development occurs. Four exemplary badlands within the Villacarly sub catchment have been
investigated.
#*
#*
#*
#*#*
#*
#*
ISABENA
ES
ER
A
Cabecera
Villacarli
Ceguera
BARASONA
Corva
Seira
Campo
Escales
Serraduy
Las Paules
Pont de Suert
275000
275000
290000
290000
305000
305000
320000
320000
4666
000
4666
000
4684
000
4684
000
4702
000
4702
000
4720
000
4720
000
rivers
Isábena catchment
Villacarli catchment
#* climate stationUTM 31 N
�
Figure 3-1: Location of the Isábena cacthment whithin the Ebro basin; yellow area = Ebro basin; red area = Isábena catchment
Figure 3-2: Location of the Isábena catchment within the catchment of the Barasona reservoir and of the Villacarli sub catchment within the Isábena catchment
15
3.2. Climate
The mountainous part of Aragon
mediates between two different
climatic regimes: the oceanic,
which dominates the Occidental
Pyrenees and the mediterranean
climate in its continental variant,
which dominates the Central
Pyrenees. The Isábena catchment
is dominated by the latter. Main
characteristics of this climate
regime are ample thermal
contrasts between the dry winter
with high insolation and the hot
summer with rainfall occurring in
high intensity storm events. The
Isábena catchment itself can
again be sub divided in a warmer
and drier part reaching from the
Barasona reservoir up to the
Turbon, the highest peak in the
Villacarli sub catchment with
2373 m a.s.l (Figure 3-2). Mean
annual temperature varies
between 11 – 14 °C.
The northern part is dominated by a colder and wetter climate regime with a mean annual
temperature of 9 – 11°C (Verdú et al. 2002). Precipitation varies between 450 and 1300 mm
and increases with altitude. The mean annual precipitation for the whole catchment amounts
to 767 mm. High rainfall intensities occur during spring and autumn. July is the month of less
precipitation.
Due to exposition, altitude and the heterogeneity of the catchment, great climatic contrasts can
be found within a short distance gradient. According to Verdú (2002), the highest
precipitation occurs in the uppermost sub catchment, the Cabecera catchment (see Figure
3-2). However, most storm events were recorded in the sub catchments of Villacarli and
Carrasquero (see Figure 3-2 and Table 3-3 ).
The highest temperatures occur in July and August while December and January are the
coldest months (Table 3-1). Frost can occur between September and May with the highest
probability in December and February. For mean monthly and annual values for temperature
and precipitation see Table 3-1 and Table 3-2, respectively.
Figure 3-3: Topographic map of the Isábena catchment.
ISABENA
16
Table 3-1: Mean monthly and annual temperatures for five stations in or near the study area in °C (Ninot et al., 1993)
Table 3-3: Rainfall intensity and total precipitation by pluviograph for all storm events during. (Verdú, 2002)
Pluviograph n° of storm events
mean intensity [mm/h]
Corva (upper catchment)
8 6.5 (+- 4.0)
Las Paúles (altiplano) 9 4.16 (+- 2.0) Serraduy (central catchment)
13 5.26 (+-3.4)
3.3. Hydrology
The Isábena river is characterized by a pluvionival hydrological regime (Verdú et al., 2002)
with runoff peaks in late spring / early summer initiated by the snow melt in the upper
reaches. Minima are reached in summer (August and September) with a slight delay to the
season with less rain (July-August). The maxima occur in autumn triggered by storm events
with mean runoff rates of 40 m³/s. Mean annual runoff is 5.7 m³/s with a standard deviation of
2.4 m²/s indicating the high interannual variability (Verdú, 2002). According to Verdú (2002),
the Cabecera catchment attributes about 60% and the Villacarli, although being an ephemeral
stream, attributes up to 20% of runoff during flood events. During storm induced flood
events, the maximum runoff lowers to the centre of the catchment to the Villacarli and the
Carrasquero catchment (see Figure 3-2).
17
3.4. Geology and geomorphology
The Isábena headwaters are cut into
granitic and metamorphic, siciciclastic or
carbonate rocks from the Paleozoic era,
which form the Axial Pyrenees. The
Isábena runs in a narrow gorge here. To
the south follows a geosynclinal mainly
filled with calcareous Cretaceous and
Palogene sediments (see Figure 3-2).
During the alpine orogeny, these have
been pressed and folded against the Axial
Zone. The resulting ranges are called the
“Internal Ranges” (Sierras Interiores). In these erodible materials as marls and sandstones,
transverse valleys could develop such as the Arroyo de Villacarli or the Carrascquero
Catchment (see Figure 3-2). In case of the Arroyo de Villacarli, a sandstone layer once
covered the Mesozoic marls. Wherever this sandstone layer has been removed, the highly
erodible marls surface and badland formation takes place. South of the Internal ranges extends
the Intermediate Depression, a basin filled with synorogene flysch, marls, and Oligocene
conglomerates. These lowlands with less inclination are used for agriculture. The southern
limit of the catchment is formed by the External ranges, which are the transition to the Ebro
basin. In some parts, they form mountain chains of over 1700 m and in other part already have
characteristics of foothills (Lautensach, 1964). They are mainly formed of cretaceous
limestone in combination with clays and conglomerates from the Cenozoic era. The Isábena
flows between two morphological units: the intra-pyrenean depression formed by the Vall de
Lierp, the Corredor de Merli and the Sierra del Chordal on the right side and the Sierra de Sis
on the left side.
3.5. Soils
The soils in the Isábena catchment are characterized by their poor development (Martinez-
Cassasnovas and Poch, 1998). Mainly Xerorthents, Litic Xerorthents on calcic slopes with
little soil depth (A-R-profile) can be found. In more stable positions and on less resistant
bedrock, Tipic Xerorthents with a A-C or A-Bw-C profiles develope. They are mostly basic
soils with a silty- loamy to sandy-loamy structure. With 2% and less, the content of organic
matter is low. Soils are well drained but have low water retention capacity due to low soil
depth. The most eroded sites are, besides the badlands, the agricultural croplands which are
often situated on steep hillslopes.
Figure 3-4: Lithology of the Ésera-Isábena-catchment (Valero-Garcés et al., 1999)
18
3.6. Vegetation and land use
The potential natural vegetation for this area can be presumed as „Carrasca“, forests of
Quercus Ilex ssp. Ballota (Ninot et al. 1993). Currently, this vegetation type only has a small,
disperse extension. The main part of the catchment is covered by more degraded vegetation
forms dominated by shrubs and herbs.
The northern part is mainly covered by Pinus sylvestris forests from 600 m. a. s. l. From 1600
up to 2300 m a.s.l. Pinus unicata dominates (Verdú et al., 2003). Deciduous woodlands are
formed by Quercus faginea, Betula pendula and Fraxinus sp.. These stand form mixed forests
accompanied by Pinus unicata. Within the whole catchment, grass communities become more
and more important as grazing ground for livestock, mainly sheep. In the southern part of the
catchment where the valley is wider and expanded floodplains have developed, agriculture
activities are the dominant land use. The main crops are wheat (Triticum aestivum), barley
(Hordeum vulgare) and sunflowers (Helianthus annuus). Permanent crops are mainly
almonds (Prunuc dulcis) and olives (Olea europea).
3.7. Socioeconomic aspects
The administrative district of Ribagorza has suffered great population losses during the 20th
century. From 13.6 inhabitants / km² at the beginning of the century, the number decreased to
5.5 inhabitants /km² in 1998. Nowadays, over 60% of the villages have less then 200
inhabitants. Only two villages have over 1000 inhabitants. The main income derives from
agro-pastoral activities; industry is of little importance. The largest proportion of the income
derived by agriculture is obtained by livestock, mainly sheep, followed by cattle and pork
(Verdú, 2003). Agricultural crops become more important in the area downstream below the
Barasona reservoir. The dam was constructed in 1932 for irrigation purposes and power
generation. It has a capacity of 92*106 m³, surface of 692 ha and a maximum depth of 60m.
The average depth is 16.5 m. The capacity of the power house is 26 MW. A channel
originating in the reservoir (Aragón and Cataluña channel) supplies 104.850 ha of cropland
with irrigation water during March to October. In former times, the reservoir was flushed
every year in order to clean out the sediment. Since the 1950s, the reservoir has no longer
been flushed regularly. As a consequence, in 1995 a layer of sediments with a maximum
thickness of 25 m near the dam (Valero-Garcés et al., 1999) occupying 16-18 km³ had
reduced the storage volume of the basin about one third. During three years, the reservoir had
to be drained completely after the irrigation period and the sediments near the dam had to be
dredged to change the plugged bottom outlets. However, most of the sediment remained in the
basin and flushing is not performed regularly (Valero-Garcés et al., 1999). The storage
volume of the basin thus constantly decreases.
19
4. Methodology This study aims at modelling erosion by runoff on badland hillslopes applying the WASA-
model. A new routine calculating sediment production based on the MUSLE (Modified
universal soil loss equation) has been introduced to the hydrological model and is tested for
the first time in this study. During a field trip, badlands in the study area were characterized
and relevant model input parameters surveyed. The remaining parameters were derived
through the application of other models and evaluation of literature. Based on these values, a
sensitivity analysis was conducted in order to identify the range within results could probably
vary. Furthermore, one parameterization was composed which is assumed to be the best
spatial representation of the modelled slopes. That configuration was applied in two variances
in order to quantify the effect of submodel disagreements between the spatial discretization of
WASA and the MUSLE approach.
The chapter is divided into an introduction to the modelling approaches, the description of the
field work and its results which are then applied for the parameterization of the model.
Modelling results will be presented and discussed in chapter 5.
4.1. Introduction to the modelling concepts
4.1.1. Introduction to the WASA-Model
WASA stands for “Model of Water Availability in Semi- Arid Environments”. It is a
hydrological model developed by Güntner (2002) for the quantification of water availability
in semi-arid environments in view of environmental changes. WASA is a deterministic model
composed of process-based conceptual approaches applied to a semi distributed spatial
discretization. The model requires a minimum of calibration of parameters which makes it
useful for impact studies in areas with low data availability.
The model is process-based in the sense that all water fluxes are represented by realistic
hydrological processes. It is conceptual though in the sense that process representation is
based on approximating and simplifying assumptions. Nevertheless WASA can be called a
physically based model for its parameters can be derived from measurable physical
characteristics of the study area (Güntner, 2002). Hydrological processes represented in
WASA by individual routines are interception, evaporation, infiltration, surface and
subsurface runoff, transpiration and ground water recharge as well as lateral distribution of
water between the different spatial units (for details see Güntner, 2002). Furthermore, WASA
20
can account for reservoirs storage, river flow and water use within a catchment. These latter
processes are not of importance for this study and are thus not described here.
Considering the spatial discretization applied in WASA, it is a semi distributed model. The
catchment is represented by discrete georeferenced spatial units down to a level below which
the spatial units are no longer georeferenced but only represented by their fraction of area
within the superior spatial unit (see Figure 4-6). The watershed being modelled is divided into
subbasins (further on referred to as SB) which represent sub catchments. Within the sub
catchment areas with a similar toposequence, lithology and soil characteristics form a
landscape unit (further on referred to as LU). Subbasins and landscape units are
georeferenced areas within the catchment being modelled. Landscape units are composed of
terrain components (further on referred to as TC) that have similar slope angles and soil
associations. Down to this scale, a distributed structure is followed. The lowest level of spatial
discretization is formed by the soil-vegetation components which result from the intersection
of soil types with landcover classes. These are no longer georeferenced but only given by
their spatial fraction of the TC they occupy. That makes WASA a semi-distributed model.
The characteristics of each soil vegetation component are given by a soil profile representing
the corresponding soil type and vegetation cover. At this level, WASA applies a lumped
concept, meaning that spatial variability is no longer represented within this lowest spatial
unit.
What makes WASA especially applicable to semi-arid areas are, among others, the two layer
evapotranspiration model applied, which accounts for energy transfer at the soil surface and
thus soil evaporation (see 4.1.2.2.). Furthermore, it is capable of displaying the high fraction
of infiltration excess surface runoff (Hortonian runoff), which is typical for runoff generated
by high intensity storm events. WASA offers the possibility to account for changes in
hydrology induced by the seasonality of plan growth due to dry and rainy seaond.
Although being applied to a rather sub-humid than semi-arid area here, WASA should still be
able to display the relevant parameters which are similar from the hydrologically point of
view. Rainfall occurs mainly in form of storm events. Seasonality is also given here with high
rainfall in spring and autumn and lower rainfall in summer and winter. Seasonality of
vegetation parameters is rather induced by changes in temperature than due to the lack of
water though. WASA permits adjusting the according file based on the relevant climate data
(see below, section 4.3.5). Vegetation cover is sparse in large parts of the Isábena catchment
and especially on the badland slopes represented in this study. Evaporation from the soil
surface thus is also an important parameter.
21
Level Type and criteria of delineation Process working on this level
1. Subbasin (SB)
• geographically referenced polygon of a sub catchment
• wherever possible delineated with the Arc Hydro tool box, or based on aerial fotographies and field measurements
• runoff routing
2. Landscape unit (LU)
geographically referenced polygon with similarities in: • major landforms
• general lithology
• soil association
• toposequence
• modelling unit with similar characteristics referring to lateral processes and similarity of subscale variability in vertical processes
• composed of 1 – 3 terrain components
• runoff response of al landscape units are summed up to give total runoff of SB
3. Terrain component (TC)
fraction of area of LU (no geographic reference) with similarities in:
• slope gradient
• slope position within toposequence
• soil association
• lateral transfer of surface and subsurface flow between TCs along the hillslope (from highlands to lowlands)
• reinfiltration and exfiltration (return flow) in TC with lower topographic position
• sediment production and lateral transfer between TCs as with runoff
4. Soil vegetation component (SVC)
fraction of area of TC characterized by specific combinations of • soils
• vegetation
• Represents the variability of soil hydraulic properties within a TC. (partial area approach for saturation-access surface runoff)
• lateral transfer of surface ad subsurface runoff of TC among all svc
5. Profile
representative profile of soil vegetation component
• calculation of water balance I the profile of each soil-vegetation component
• determination of vertical and lateral water fluxes for individual horizons
Figure 4-1: Hierarchical multi-scale disaggregation scheme for structuring river basins into modelling units in WASAFigure taken from Güntner (2002) with permission.
22
4.1.2. Process representation
In the following section, sub models of WASA representing the hydrological processes are
described roughly to give an overview. For detailed description see Güntner (2002). It will be
limited to the processes on the hillslope which are relevant for this study and omit processes
dealing with deep groundwater recharge, processes in the river network or in reservoirs.
4.1.2.1. Interception model
The interception model integrated in WASA is a simple bucket approach (see Eq. 4-1). The
interception storage depending on the leaf area index (LAI) and a given maximum height for
the water film on the leaves. For this study the maximum height is set to 0.03 mm. Rainfall
over the canopy is added to this storage until it is filled. Excess water is assumed to reach the
soil surface and thus added to the infiltration routine. The maximum height of the water film
might appear high but this accounts for the fact that currently, daily time steps are calculated
underestimating processes as evaporation and refilling over the day.
Eq. 4-1: Simple bucket approach for the representation of interception
111tt EPII −−−−++++==== −−−−
It Water in interception storage at time step t [mm]
P Precipitation [mm]
PI Intercepted precipitation [mm]
Ei Evaporation from interception storage [mm]
4.1.2.2. Evapotranspiration model
Evapration from open water bodies and the interception storage is described by a simplified
form of the classical Penman – Monteith approach (Penman (1948); Monteith (1965)) (see
Eq. 4-2).
For the representation of total evapotranspiration the two-layer approach from Shuttleworth &
Wallace (1985) is applied, consisting of a model for plant transpiration and evaporation from
soil surface (only applied to the upper most horizon) (see Eq. 4-3 to Eq. 4-5). These
components are determined separately but interrelated by the vapour pressure deficit of the
air. Evapotranspiration is characterized by nonlinearity during day and night. To consider this
phenomenon, a concept of Schulla (1997) is applied to the input data on daily basis dividing it
into a daytime and a nighttime period. Currently, this is simply done by dividing it into two
twelve hour time steps, an assumption that is valid for the study area near the equator treated
23
by Güntner (2002). For the study area in Spain, a dynamic approach should be integrated to
represent changing day length over the year. Energy input as driving force to this system is
net radiation in [W/m²]. For more detailed description of parameters see Güntner (2002), pp.
38 – 40.
Eq. 4-2: Simplified Penman-Monteith approach for simulating evaporation from the interception storage and open water bodies (Penman, 1948; Monteith, 1965)
(((( ))))
++++++++
++++====
aa
cs
aap
PMr/r1
r/DcAtE
λλλλ∆∆∆∆
ρρρρ∆∆∆∆
λλλλ
Epm Evapotranspiration [m / time step]
t Number of seonds per time step [-]
λ Latent heat of vaporization of water [J / kg]
∆ Gradient of the saturated vapour pressure curve
[hPa / K]
A Available energy [J / ms] = [W / m²]
ρ Density of air [kg / m³]
dp Specific heat of moist air [J / kg K]
D Vapour pressure deficit at referece level
[hPa]
aar
Aerodynamic resistance [s / m]
csr
Canopy resistance [s / m]
γ Psychrometric constant [hPa / K]
Eq. 4-3: Two-layer approach for the estimation of evapotranspiration after Shuttleworth and Wallace (1985)
ST EEE ++++====
Eq. 4-4: Plant transpiration
(((( ))))
(((( ))))
++++++++
++++−−−−====
ca
cs
camps
Tr/r1
r/DcAAtE
γγγγ∆∆∆∆
ρρρρ∆∆∆∆
λλλλ
Eq. 4-5: Evporation from soil
(((( ))))
++++++++
++++====
sa
ss
samps
Sr/r1
r/DcAtE
γγγγ∆∆∆∆
ρρρρ∆∆∆∆
λλλλ
24
ET Plant transpiration [mm]
ES Soil evaporation [mm]
AS Available energy at the soil surface [J/m s]
Dm Vapour pressure deficit inside the canopy
[hPa]
car Bulk boundary layer resistance
which controls the transfer between leaf surface and hypothetical mean canopy air stream at height zm
[s/m]
sar Aerodynamic resistance controlling
transfer between soil surface and zm
[s/m]
ssr Soil surface resistance [s/m]
4.1.2.3. Infiltration model
The infiltration module is based on an adaptation of the Green-Ampt approach by Peschke
(1977, 1987) and Schulla (1997) (see Güntner, 2002; pp. 41). The routine is applied at the
level of soil vegetation components. Input to the routine is precipitation (P) reduced by
interception (PI). This amount is increased by lateral surface inflow from higher TCs (Rs,TC)
and other soil vegetation components within the TC currently computed (Rs,SVC). To capture
runoff from SVCs within the same TC, two iterations of Eq. 4-6 have to be conducted. During
the first run, Rs,SVC is set to 0. Possibel runoff is then redistributed between all SVCs.
Afterwards real infiltration for all SVCs is calculated.
Eq. 4-6: SVC,sTC,sIF RRPPR ++++++++−−−−==== (all in mm/∆t)
The infiltration procedure starts by calculating the moment of time (ts,i) when the input rate
(RF) is higher than the saturated hydraulic conductivity (ks,i). ts,i is calculated according to Eq.
4-7). This is the moment, when saturation at the soil surface is reached. Is ts,i smaller than the
modelling time step, the whole rainfall infiltrates into the soil. Saturation at soil surface is not
reached. From ts,i on, infiltration rate decreases approaching its limiting value ks,i at the end of
the modelling time step (see Eq. 4-11 and Eq. 4-12). If I = 1 (uppermost horizon) and RF
exceeds Fi, the difference between both parameters describes the amount of infiltration excess
runoff, or Hortonian Runoff (Horton, 1933).
The routine ends here. Only if the depth of the wetting front suction (ds,i) reaches below the
lower limit of horizon i, or the entire refillable porosity of horizon i had filled up, the next
lower horizon would be taken into account. In both cases, the horizon would be saturated
within ts,i but following Eq. 4-13 instead of Eq. 4-7 and setting ds, in Eq. 4-8 equal to dh,i.. No
25
saturation excess is produced. Subsequently, this procedure is repeated for all lower horizons
until at one step infiltration excess is produced or all input is infiltrated. Saturation at the soil
surface is produced, if all upper horizons plus the current horizon are saturated before the end
of the time step being modelled.
The scaling is one of the few calibration parameters in WASA. It is introduced to balance the
underestimation of rainfall intensities by daily rainfall data. If used in this way, a ratio of
average high resolution rainfall data to average low resolution rainfall data used in the model,
describes it best. The factor can also be applied for adjusting the infiltration routine
accounting for the high spatial variability of infiltration due to surface crusts, macropores and
so on. In this study, it is set to 1.
Eq. 4-7: Fi,si,s R/Ft ====
Eq. 4-8: i,ai,si,s ndF ⋅⋅⋅⋅====
Eq. 4-9: (((( )))) 1s/k/R
dFi,sF
i,f
i,s−−−−
====ψψψψ
Eq. 4-10: ii,ti,a nn θθθθ−−−−====
Fs,i Infiltration volume until ts,i [mm]
Fi Infiltration volume of whole time step [mm]
ds,i Depth of wetting front below top of horizon i at time ts,i
[mm]
dh,i Depth of horizon i [mm]
na,i Refillable porosity of horizon i [-]
nt,i Total porosity of horizon i [-]
Θi Internal water content of horizon i [Vol%100][-]
Ψf,i Suction at wetting front of horizon i [mm]
ks,i Saturated hydraulic conductivity [mm/∆t]
sF Scaling factor [-]
i Index for soil horzon currently computed [-]
Eq. 4-11:
i,s
i,s
ii,si,si F
cF
cFlnc)tt(FF ++++
++++
++++⋅⋅⋅⋅++++−−−−====
Eq. 4-12:
i,fi,anc ψψψψ⋅⋅⋅⋅====
Eq. 4-13:
Fi,ai,hi,s R/)nd(t ⋅⋅⋅⋅====
26
4.1.2.4. Soil water model
The soil water model describes the soil moisture at each time step for each horizon. It
balances incoming and outcoming fluxes. The incoming fluxes are infiltration according to
section 4.1.2.3, lateral subsurface flow from higher TCs and SVCs within the same TC and
percolation from upper horizons. The outgoing fluxes are evaporation from the soil surface
(see section 4.1.2.2) which only takes into account the uppermost horizon. Transpiration (see
section 4.1.2.2) is applied to the whole rooting zone by weighting every horizon according to
its fraction of field capacity in relation to the total field capacity of the entire routed zone.
Furthermore percolation to the lower horizon or deep groundwater and outgoing lateral
subsurface flows to other SVCs of the same TC or lower TCs have to be mentioned.
Whenever the actual water content exceeds water content at field capacity, water for outgoing
fluxes is available.
Percolation depends on the hydraulic conductivity (unsaturated) of the soil. It can be limited
by the refillable porosity or the saturated hydraulic conductivity of the lower horizon or of the
bedrock when treating the lowest horizon of the profile.
Lateral flow is described by the Darcy equation (see Eq. 4-14). Hydraulic gradient is given by
the slope of the corresponding TC. Runoff routing from SVC to SVC is done between
horizons of more or less the same depth. If a profile is too shallow, the additional input is
added to the next higher horizon. Excess water is added to the surface runoff of a SVC.
.Eq. 4-14:
TCi,sq skA ⋅⋅⋅⋅====
4.1.2.5. Lateral distribution of surface and subsurface flow between soil vegetation components
Runoff generated on a SVC is divided into flow to the lower TC and flow to the adjacent
SVCs. The amount of runoff routed to a lower TC is determined by the fraction of area, the
SVS occupies within a TC.
Runoff is evenly distributed between al SVCs although they are not necessarily connected for
they do not represent georeferenced, discrete areas but the statistical fraction of a combination
of soils and vegetation. They do not represent an area but rather patches.
Runoff distribution is performed according to the fraction of area of the receiving SVC within
its TC (see Figure 4-2). This distribution pattern is also applied to subsurface runoff.
Wherever possible, subsurface runoff is routed to a horizon of similar depth below ground
27
surface. If the soil subsurface runoff is routed into is too shallow or reaches saturation, surplus
us added to surface runoff as return flow (see 4.1.2.4).
Eq. 4-15:
(((( ))))∑∑∑∑====
⋅⋅⋅⋅====n
1xx,SVCSVCTC aQQ
Figure 4-2: Lateral distribution of runoff between soil vegetation components on one TC. (Figure taken from Güntner (2002); with permission)
4.1.2.6. Lateral distribution between TCs of surface and subsurface runoff
A fraction of surface runoff is directly transferred into the river (Eq. 4-16) representing
concentrated flow in rills. The amount of water directly contributed to the river is calculated
by the fraction of area the corresponding TC occupies within the sum of its own area and the
lower TCs. At each step, the area of reference is composed of the TC currently computed plus
the lower TCs. In case of the lowest TC the reference area is just the area of the TC itself.
Runoff output is thus completely transferred into the river.
The rest of the output is divided between all lower TCs according to their fraction of area (see
Eq. 4-17) within the LU. Surface Runoff production at the level of landscape unit is calculated
by summing up the direct output of the upper TCs (rill flow9 plus the output of the lowest TC.
Subsurface runoff is completely transferred to the next TC and then equally distributed among
all SVCs.
28
Eq. 4-16:
∑∑∑∑∑∑∑∑====
⋅⋅⋅⋅====
m
1xm
x
x,TC
x,TCx,TCriver
a
aQR
Eq. 4-17:
∑∑∑∑∑∑∑∑
−−−−
====
⋅⋅⋅⋅====
1y
1xm
x
x,TC
y,TCx,TCy,TC
a
aQR
aTC Fraction of area of TC in landscape unit
x Index of TC which is runoff source are for flow to be redistributed
y Index of TC which is runoff sink area of redistributed flow
m Number of TCs within a landscape unit
Figure 4-3: Lateral transfer of water and sediment from higher to lower TC. TC = Terrain component, the number indicates the position within the landscape unit. (1= highland, 2 = slope, 3 = lowland), taken from Güntner, 2002, with permission.
29
4.1.3. The Modified Universal Soil Loss Equation
4.1.3.1. Introduction to the Modified Universal Soil Loss Equation
Within the SESAM project, the WASA-Model has been extended by new routines describing
the sediment transport at the three different levels the model works: on the hills, in the river
network and in reservoirs. The sediment-transport routine for the hillslopes, which is
investigated in this work, is based on the MUSLE approach (Modified Universal Soil Loss
Equation) by Williams (1975) (see Eq. 4-18). It is, as the USLE (Universal soil loss equation,
by Wischmeier and Smith (1978)) an empirical equation based on the evaluation of field
measurements acquired predominantly on agricultural fields in North America. The MUSLE
offers several advantages over the USLE especially when working at the level of catchments.
Instead of rainfall energy, the energy input to the MUSLE is a runoff variable composed of
the surface runoff and the peak runoff rate (see Eq. 4-18). This allows the application to
individual storm events (Williams, 1995). Furthermore, it eliminates the need of a sediment
delivery ration necessary in the USLE. Using runoff as energy component increases the
accuracy of sediment yields because runoff accounts for more variation in soil erosion than
rainfall (Smith et al., 1984).
Currently, the MUSLE is applied at the level of TCs, a subunit of the catchment to account
for spatial variability of hydraulic properties of soil and vegetation. The MUSLE implies a
nonlinear relationship between the area and slope length of the spatial unit it is applied to and
sediment production. Sediment production is routed linearly though between the TCs along
the hillslope though. The division of hillslopes into spatial subunits in combination with linear
routing of sediment, as it is currently done in WASA and other spatially distributed models,
(e.g. SVAT, see Chen and Mackay, 2000) is not in agreement with this integrated approach of
the MUSLE designed for entire hillslopes. Area and slope length, both factors changed by
different spatial distributions, are in nonlinear relationship with the output of the equation –
sediment production.
The quantification of the effect this disagreement of sub model assumptions has on sediment
production is one of the tasks dealt with in this study (see section 4.3.2 and 5.3).
Eq. 4-18: Modified universal soil loss equation after Williams, 1975
ROKFLSPCK)areaq(Q11.8sed USLEUSLEUSLEUSLE0.56
tcpeaksurf ⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅====
30
Sed sediment yield (t/ha)
Qsurf surface runoff volume (mm/ha)
qpeak peak runoff rate (m³/s)
area area of the terrain component m²
KUSLE USLE soil erodibility factor after Williams, 1995
cmtonm
hrmt013.03
2
⋅⋅⋅⋅−−−−
⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅
CUSLE USLE cover and management factor [-]
PUSLE USLE support practice factor [-]
LSUSLE USLE topographic factor (-) [-]
ROKF coarse fragment factor (-) rock)0053.0(exp ⋅⋅⋅⋅−−−−
Qsurf is generated in the hydrological routine of the WASA-Module. The peak runoff rate (qpeak) reads
Eq. 4-19:
conc
tcsurfconc_t
peakt6.3
AQq
⋅⋅⋅⋅
⋅⋅⋅⋅⋅⋅⋅⋅====
αααα
αt_conc amount of rainfall during tconc [mm] )1log(t2 5.0concexp1
αααα−−−−⋅⋅⋅⋅⋅⋅⋅⋅−−−−
Atc area of Terrain component [m²] GIS
tconc time of concentration [h]
Q
TC
v3600
l
⋅⋅⋅⋅
α0.5 fraction of daily precipitation that falls within 30 min
[mm/0.5h] 0.21
lTC absolute slope length of TC [m] GIS
vQ overland flow velocity [m/s] 6.0nmanning/3.0
TCslope4.0ovq
⋅⋅⋅⋅
qov average overland flow rate on a 1 m strip
[m3/s]
6tc
TCtin_sufout_surf
10A2
l3600d)qq(
⋅⋅⋅⋅⋅⋅⋅⋅
⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅++++
dt Time step in [h] 24
qsurf_out surface runoff towards lower TC
[m³] See section
qsurf_in surface runoff from upper TC [m³]
31
Kusle originally depended on the content of organic material, soil structure and soil
permeability. Willams (1995) proposed a new approach reading:
Calculation of the KUSLE factor Neitsch et al. 2002
Eq. 4-20: hisandorgsiclcsandUSLE ffffK ⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅==== −−−− with
−−−−⋅⋅⋅⋅⋅⋅⋅⋅−−−−⋅⋅⋅⋅++++====
100
m1m256.0exp3.02.0f silt
scsand
a factor that reduces soil erosion for soils with a high content in coarse sand
3.0
siltc
siltslcl
mm
mf
++++====−−−−
a factor which leads to low erodibility for soils with high clay to silt ratio
[[[[ ]]]]
⋅⋅⋅⋅−−−−++++
⋅⋅⋅⋅−−−−====
orgC95.272.3exporgC
orgC25.01forg
a factor that reduces erodibility for soils with a high content in organic carbon
−−−−⋅⋅⋅⋅++++−−−−++++
−−−−
−−−−⋅⋅⋅⋅
−−−−====
100
m19.2251.5exp
100
m1
100
m17.0
1fss
s
hisand
a factor which reduces erodibility for soils with extremely high sand contents (Neitsch et al. 2002)
These calculations are based on particle size classes as used in the US soil taxonomy. Sand
ranges from 2 to 0.05 mm, silt from 0.05 to 0.002 mm and clay is smaller than 0.002 mm
(Brown, 2003)
CUSLE is the cover and management factor that accounts for reduction in soil erosion by
vegetation cover or residue left on the field. On the badland slopes, this value is set to 1,
representing maximum erosion. For the other soil vegetation components the value is derived
by multiplying the value for the corresponding vegetation cover and the value for the
corresponding tillage method (see Stone, 2005). PUSLE is the support and practice factor
describing the ratio of soil loss ascribed to a specific support practice to the corresponding
loss with up-and-down slope management. Support practices would be stripcropping, counter
tillage and terrace systems. Since no such practices could be observed in the field, the factor is
set to the maximum of 1 on the badland slopes and 0 on vegetated slopes. For agricultural
crops, the corresponding values were inserted (see Neitsch et al., 2002).
The topographic factor (LSUSLE) is described by the following equation:
32
Eq. 4-21: topographic factor of the MUSLE
(((( ))))(((( ))))065.0sin56.4sin41.651.22
LLS hillhill
2
m
hillUSLE ++++⋅⋅⋅⋅++++⋅⋅⋅⋅⋅⋅⋅⋅
==== αααααααα
with Lhill Slope length [m]
m Exponential term [[[[ ]]]](((( ))))slp835.35exp16.0m ⋅⋅⋅⋅−−−−−−−−⋅⋅⋅⋅====
slp Slope [m/m] (rise over run)
αhill Slope angle [°]
hilltanslp αααα====
Slope length in WASA is initially given by the mean slope length of the landscape unit. Slope
length for the TC is computed as a weighted fraction of the original slope length according to
the fraction of area the corresponding terrain component occupies within the landscape unit
and its slope.
4.1.3.2. Lateral distribution of sediment
The soil erosion routine is applied on the level of TCs. Other than the hydrological routines, it
is not applied to every SVC but mean values of all SVCs within a TC weighted by their
fraction of area are calculated and applied to the MUSLE.
Sediment generation is not represented in the sum of its processes but my means of an
empirical equation that cannot account for additional sediment input from upper TCs. To
avoid an overestimation of erosion through sediment input from upper TCs, two additional
limit modes were implied in WASA:
• a limit based on the transport capacity of runoff according to Govers (1990) and Morgan et al. (1998).
• a limit based on the sediment produced on the corresponding area assuming maximum erodibility (K=0.5) (see 0.).
The first one is a process-based approach based on the transport capacity after Govers (1990)
and Morgan et al. (1998) (see Eq. 4-22). Is the sediment concentration higher than the
transport capacity, the rest of the sediment remains on the TC representing resdeimentation.
The second approach compares the sum of incoming sediment and sediment produced on the
TC with the erosion rate calculated for the corresponding TC and its configuration but with
KUSLE (erodibility factor) set to the maximum of 0.5 cmtonm
hrmt013.03
2
⋅⋅⋅⋅−−−−
⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅.
33
Transport capacity according to Govers (1990) and Morgan et al. (1998)
Eq. 4-22 :
(((( ))))ηηηηϖϖϖϖϖϖϖϖ crcTC −−−−====
TC transport capacity c experimentally derived coefficient − 6.0
50 ]32.0/)5d[( −−−−++++
ω unit stream power [cm/s] sv100 ov ⋅⋅⋅⋅⋅⋅⋅⋅
vov velocity of overland flow [m/s]
6.0nmanning/3.0
TC4.0
ov slopeq ⋅⋅⋅⋅
qov average overland flow rate [m³/s] 6tc
TCtin_sufout_surf
10A2
l3600d)qq(
⋅⋅⋅⋅⋅⋅⋅⋅
⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅⋅++++
manningn Manning coefficient of roughness [m173/s] Values from literature, Neitsch et al. (2002)
Atc area of terrain component [m²] See section 4.2.1.2 for derivation
ωcr critical value of unit stream power [cm/s] 0.004 m/s
s slope [%] See section 4.2.1.2 for derivation
η experimentally derived coefficient − 25.050 ]300/)5d[( ++++
d50 median particle size of soil [µm] Computet within WASA
lTC absolute slope length [m] See section 4.2.1.2 for derivation
dt time step [h]
In case of the sensitivity analysis, sediment transfer was not applied which is not of relevance
due to the fact that the spatial discretization applied used only one terrain component per
badland (see section 4.3.1). For the other two spatial discretizations, 4 different combinations
of routing and transfer mode were applied (see Table 4-1).
Mode A omits sediment transfer between TCs and allows unlimited erosion. Mode B, C and
D all transfer sediment from upper to lower TCs along the hillslope but have different
transport limits. Mode B has, as mode A, no transport limit. It allows maximum erosion.
Mode C is limited by the transport capacity of runoff and Mode D is limited by the amount of
sediment production computed with maximum erodibility. Mode A was applied in spite of
having more than one terrain component on BL1, BL3 and BL4 in order to quantify the effect
of sediment transport at the level of terrain components and to test weather or not erosion
rates represent the spatial variability of soil and vegetation factors.
34
Table 4-1: Routing and transport modes for sediment applied during this study
Case Routing mode Transport mode
A no sediment transfer between TCs no transport capacity limit
B sediment transfer between TCs no transport capacity limit
C sediment transfer between TC transport capacity according to Govers, 1990; Morgan et al., 1998
D sediment transfer between TC transport capacity = max. soil erosion after MUSLE equation, K = 0.5
4.2. Field work
During twelve days of field work (01.09.-12.09.05), the specific characteristics of badlands in
the Isábena catchment were investigated. As mentioned before, various authors have
identified the badlands in the sub catchment of the Arroyo de Villacarli as the main sediment
source responsible for the siltation of the Barasona reservoir (Valero-Garcés et al. 1999).
The field campaign aimed at getting an overview of the morphological and hydrological
processes acting on the badland slopes. It was tried to characterize the badlands by relevant
parameters and in addition, data was collected which was used for the parameterization of the
model in order to compute sediment and soil production and transport along representative
hillslopes.
4.2.1. Survey
4.2.1.1. Description
The investigation aimed at detecting spatial variation of parameters relevant for model
parameterization on the badland hillslopes. Four exemplary badlands, characteristic for the
badlands occurring in the study area, situated in the Arroyo de Villacarli (see Figure 4-4 and
Figure 4-5) were chosen to conduct the survey. Additionally, more detailed investigations
were carried out on one badland of optimal size and accessibility. Measurements were
conducted from within the ephemeral channels of the badlands. The main channels were
followed and every 50 (BL11 and BL2) or 150 steps2 in case of the larger badlands 3 and 4 the
following parameters were mapped:
1 BL = badland, used when referred to one of the four study sites 2 one step = ca. 0.7 m
35
• Slope angle of the left and right slope facing upstream in the internal gully. The data was recorded in percent by means of a handheld inclinometer
• Aspect is measured by means of an electronic compass in built in the Garmin etrex summit GPS-device
• Vegetation cover was estimated in percent considering a strip from the ridge to the gully of about 2 m width and roughly described using the categories “bush”, “tree”, “grass” and “herbaceous”
• Width of the gully was measured with measuring tapes
• Outlines of the edges were measured with two Garmin etrex summit GPS-devices as far as possible. The missing data was endorsed by air photographs which are available at a scale of 1:5000 (M.A.P.A, 2005) and processing in a geographical information system.
Figure 4-4: the four catchments of the badlands used for modelling spatial discretization 3 and 3. (Aerial picture form Sept. 1982, taken by I.G.N.)
Figure 4-5: The Villacarli sub catchment with the four study sites
4.2.1.2. Results
BL1 is situated on the northern side of the Villacarli and is exposed to south-southeast (see
Figure 4-5). It is shaped like a caldera and has two main internal channels of about 60 m
length. It is the smallest of the four badlands. The surrounding vegetation is a Mattoral,
formed of bushes, smaller trees, grasses and herbs, with a vegetation cover of about 90%. A
relatively large fraction of the actual badland slopes is covered with shrubs and grasses on a
shallow soil. On the bare slopes, no soil development can take place due to the high erosion
rates. A regolith layer with a mean depth of 15 cm covers the grey marls. The badland extends
36
over 4000 m² with a mean slope length of 70.68 m and a mean slope angle of 68.61 %. Its
pediment is large in comparison to the rest of the badland (see Figure 4-6 and Table 4-6).
The other three badlands are located on the southern side of the valley. BL2 has a similar
form as BL1. The extension is about 40677.73 m², but the actual surface of the slope is larger
than in case of BL1 due to the steeper (101.33 %) and longer (133.36 m) slopes (see Table 4-2
and Figure 4-6). It is situated right next to the course of the Arroyo de Villacarli near its
confluence with the Isábena (see Figure 4-5). No real pediment can be differentiated.
Surrounding vegetation is a mixed, dense forest. The mesoclimate seems to be wetter than on
the northern side of the valley assuming by the mosses growing on branches and leaves (see
Figure 4-7). The slopes have only sparse vegetation cover.
BL3 and BL4 are long stretched out along one main ephemeral channel of about 1.5 km
length which is directly connected to the Arroyo de Villacarli (see Figure 4-6). In the lower
third, the channel forms meanders. In between those, stable pediment areas have developed
that bear vegetation and only seem to be flooded during extreme flood events. This
phenomenon is less pronounced in BL4 than in BL3. The upper channels are narrower and
deeper. West of BL3, agriculture is practiced, while the rest of the surrounding area within the
sub catchment of BL3 is covered by coniferous forest. Vegetation on the badland slopes
themselves is also very sparse. The comparison of the mean slope angle (see Figure 4-8)
between the four badlands shows that exept for BL3, the eastern slopes have a higher
inclination than the western slopes. The variation between the different badlands is bigger
then between the eastern and western slopes, though. (see Figure 4-8). Figure 4-9 shows the
mean vegetation cover which is clearly higher on the western than on the eastern slopes. In
general, vegetation cover is higher on the southern side of the valley, i.e. on the north facing
slope. In contrast to the observations from the Vallcebre catchment where less vegetation
cover was found on the north facing slopes due to freezing (Regüés et al., 1995), in the
Villacarli valley, the humidity on the north facing slopes seem to favour plant growth.
The badlands studied here belong to the humid type. Sporadical pipe erosion has been
observed but is not as dominant as on other badlands (see Romero Díaz et al. 2006). Only
small mass movements were observed during field work but the huge bolders in the channels
of the larger badlands suggest that bigger events do occur (see Figure 2-1).
37
BL1 BL2 BL3 BL3
Figure 4-6: The four study sites. In green their outer limitation, in red the main channels. Aerial fotography by I.G.N. 1982.
Table 4-2: Main characteristics of the four Badlands
Badland 1 Badland 2 Badland 3 Badland 4
Area [km²] 40000 40677.73 266200 296800
Slope [%] 68.61 101.33 71.66 81.45
Slope length [m]
39.99 93.747 69.3 76.14
Aspect SSE NE NNE NNE
Surrounding vegetation
Matorral Dense forest
Coniferous forest
Coniferous forest
Figure 4-7: Mosses and lichens found in the forest around BL2 on a north facing slope.
38
0.00
20.00
40.00
60.00
80.00
100.00
120.00
slo
pe %
eastern slope 68.61 107.67 74.69 83.55
w estern slope 71.39 95.00 68.63 79.36
standard deviation 16.00 25.70 16.42 10.50
standard deviation 13.89 14.18 25.99 16.84
BL1 BL2 BL3 BL4
0
10
20
30
40
50
ve
ge
tati
on
co
ve
r [%
]
eastern slope 25.50 4.00 19.66 14.40
western slope 44.53 17.33 42.25 47.09
standard deviationeast
35.17 13.57 40.30 28.06
standard deviationwest
35.17 13.57 40.30 28.06
BL1 BL2 BL3 BL4
Figure 4-8: Mean slope and standard deviation of the four exemplary badlands
Figure 4-9: Comparison between mean vegetation cover of slopes
4.2.2. Detail study
4.2.2.1. Description
4.2.2.1.1. Choice of the study site
As can be seen in Figure 4-11 (left side), the course of the Villacarli River once cut the slopes
of BL1. In the mid 1980s the street was regulated and with it the river. Therefore, nowadays a
dam the street was built on delimits the catchment of BL1 (see Figure 4-11, right side). The
only outlet is a culvert which was filled half with sediments during the field work in
September 2005. Although water drains through the dam during heavy storm events, it still is
an effective sediment trap. Estimating the amount of sediment accumulated behind the dam
since its construction would allow estimations of erosion rates during the past 20 years
(currently done within the SESAM project). In addition to this favourable situation, BL1 is
easily accessible, not too large and still allows the monitoring of the important processes
acting on the slopes. Therefore, BL1 was chosen for the detail study consisting of in situ
measurement of soil hydraulic parameters and numerous soil samples. It is also predestined
for instrumentation which is planned for anotother field campaign within the SESAM project.
39
4.2.2.1.2. Infiltration measurements
The measuring device used for the infiltration
measurements is a hood-infiltrometer, model UGT
Münchenberg (see Figure 4-9). The hood is connected to
a Mariotte apparatus which assures a steady state flow
while a constant hydraulic potential at the boundary layer
between soil and water is maintained. No contact layer of
sand has to be applied as necessary for other measuring
devices. Measurements on the badland slopes proved to
be difficult in the field for the hood has to be set up in a
horizontal position. On the badlands this could only be
assured measuring on a ridge or by levelling the soil
which disturbs natural soil surface conditions. The results
of the measurements conducted on the badlands are thus not trustworthy.
A steady state flow results from the measurement. For calculation of the saturated hydraulic
conductivity (kf), measurements under at least two different potentials are necessary.
Potentials of zero and one were applied during this campaign. Wherever possible, the
measurement was repeated in 30 cm below the natural soil surface. In addition, a soil sample
was taken with a 100 cm³ ring cylinder at most sample sites for determination of bulk density
and soil texture analysis. The saturated soil hydraulic conductivity can be calculated by
applying equations proposed by Gardener (1958) (see Eq. 4-23) and Wooding (1968) (see Eq.
4-24).
Eq. 4-23: Hydraulic conductivity after (Gardner, 1985) )h(
Table 4-3 shows the saturated hydraulic conductivity for the measured infiltration rates
according to the different soil types found on BL1. Values are highly variable and especially
for the badland slopes, the most important unit of this study, the measurements with the hood-
infiltrometer seem to overestimate infiltration with a mean value of 8876.44 mm/d. Regües et
al. (2000) mention rates of 512 mm/d on badland slopes in north eastern Spain. To back up
the measured values ks was also estimated with the ROSETTA model (Shaap, 2000). By
means of pedotransfer functions, the model predicts water retention after van Genuchten
(1980) (see Eq. 4-27) and estimates saturated hydraulic conductivity from soil textural data
and bulk density, if available. That allowed to include some of the soil samples of the detail
study (see below), therefore for model parameterization, the mean values estimated by the
ROSETTA model were applied although ROSETTA underestimates ks (see Table 4-3). Only
in case of the regolith on the badland slopes, infiltration according to Regüés et al. (2000) was
assumed.
.
41
Table 4-3: Saturated hydraulic conductivity measured on badland slopes and derived by pedotransfer functions applying the ROSETTA model (Shaap, 2000). Sample ID is composed of the measurement number and the depth in which it was
conducted. 0 = on natural soil surface, 30 = 30 cm below soil surface
Soil type Sample ID ks [mm/d] measured
ks [mm/d] ROSETTA
5_0 417 No sample
6_0 1446 No sample
9_0 18663.9 111.58
10_0 14978.0 11.25
mean_0 8876.44 61.41
s.d._0 9305.72 70.94
5_30 7692.33 113.53
6_30 372.88 121.54
mean 15 7054.97 117.54
Regolith on bare badland slopes
s.d. 5175.63 5.66
13_0 4212 353.91
14_0 Not valid 115.62
mean_0 4212 234.76
Badland slope with vegeation
s.d._0 - 168.50
2_0 0 No sample
3_0 0 99.1
4 Not valid 99.64
Mean_0 0 99.37
s.d. - 58.34
4_30 214 182.15
Mean_30 - -
Pediment
s.d._30 - -
1_0 13219.93 510.29
8_0 14145 232.74
11_0 9580 3736.27
12_0 9220 119.64
Mean_0 11541.17 1149.73
s.d._0 2505.34 1732.15
1_30 4168 128.26
11_30 6960 197.35
12_30 838 195.75
Mean_30 3988.75 173.79
highlands
s.d.30 3065.26 39.43
42
Eq. 4-27: Water retention after van Genuchten (1980)
n/11n
rsr
])h(1[)h(
−−−−++++
−−−−++++====
αααα
ΘΘΘΘΘΘΘΘΘΘΘΘΘΘΘΘ
Θ(h) Water content Θ [cm³/cm³] at a certain water pressure head h [cm]
Θr Residual water content [cm³/cm³]
Θs Saturated water content [cm³/cm³]
α Curve shape parameters [1/cm]
n Curve shape parameters
4.2.2.1.3. Soil sampling and analysis of samples
Soil texture is necessary for the derivation of most of the soil hydraulic parameters required
by WASA. Therefore, 35 soil samples were taken from gullies, slopes (with and without
vegetation) and ridges to detect spatial variability of soil hydraulic properties (for sampling
design, see Figure 4-11). These samples were analyzed in the laboratory of the Institute of
Geoecology at the University of Potsdam. Soil texture was determined by wet sieving for the
particle sizes coarse sand (<2 mm – 0.63 mm), medium sand (<0.63 mm – 0.2 mm) and fine
sand (0.2 mm – 0.063 mm). Coarse silt (<0.063 mm – 0.02 mm), medium silt (<0.02 mm –
0.0063), fine silt (<0.0063 mm – 0.002 mm) and clay (< 0.002mm) were determined by
analyzing 50 ml of soil suspension in a diffractometer. The suspension was collected at the
very beginning of the sieving process at the outlet of the sieving machine.
In addition, electrical conductivity and pH (in H2O) were measured. For the measurements of
pH 10 g of fine soil (< 2 mm) were suspended with 25 ml of distilled water and left over
night. Before measuring the pH, the soil was suspended again.
Organic substance was estimated following the instructions of the AG Boden (1994). The
regolith on the badlands has less than 1 mass percent. The soil on the highland has 2-4 % and
the soil on the pediment as well as on the slopes with vegetation cover has 1-2 % content of
organic matter.
43
Figure 4-11: Left: Aerial photography of BL1 taken in right: Aerial photography (M.A.P.A. 2005) showing Badland 1 which has been studied in detail. Crosses mark the sample localities where the soil samples were taken during the detail study
4.2.2.2. Results
Figure 4-12 shows the mean grain size distribution for the four geomorphological units
“edge”, “slope”, “slope with soil” and “gully”. In all cases, over 50 % are composed of fine
silt or clay. The edge and slope samples even show a content of over 75% clay and silt. At the
slopes with vegetation and in the gullies, the content of sand increases. The higher sand
content on the vegetated slopes probably derives from rests of the sandstone layer that once
covered the marls. The higher contents in the channel might indicate selective erosion.
pH varies very little over the whole area of BL 1 whereas the electrical conductivity ranges
between values from 901 to 2320 µs/ cm (see Table 4-4). The maximum value is a single
outlier taken on what seemed to be a salty crust. By eliminating this value, mean electrical
conductivity becomes 1161.58 µs and standard deviation 295.83 µs.
44
0.0
0.2
0.4
0.6
0.8
1.0
fracti
on
clay % 31.83 17.03 30.04 26.02
fine silt % 46.38 31.71 45.02 38.93
medium silt % 18.16 22.12 20.15 18.01
coarse silt % 0.00 0.67 0.00 0.01
fine sand % 3.01 15.74 3.39 7.84
medium sand % 0.60 7.67 0.80 6.07
coarse sand % 0.00 5.05 0.60 3.11
edge slope (with vegetation) slope (bare) gully
Figure 4-12: Mean grain size distribution for the four geomorphological units
Figure 4-13: Particle size distribution of soil samples taken on badlands
Table 4-4: Results of chemical soil analysis
pH (H2O) Electrical conductivity [µs/cm]
Max. 7.92 901
Min. 7.42 2320
Mean value 7.66 1127.41
Standard deviation 0.15 352.92
Variation coefficient 0.02 3.19
45
4.3. Parameterization of the WASA-Model
During this study, three different spatial discretizations were applied. Spatial discretization 1
is the simplest approach which was applied for the sensitivity analysis. Spatial discretization 2
is assumed to be the best representation of the considered sub catchments. Spatial
discretization 3 is a slightly modified version of spatial discretization 2, testing the hypothesis
that the MUSLE approach does not support the spatial discretization as applied in the WASA
model.
The derivation of parameters will be described explicitly. Values will be mentioned
exemplarily for the most important spatial unit, TC2 representing the badland slopes. The
complete parameterization can be found on the CD in form of Access data bases.
4.3.1. Spatial discretization 1 – the sensitivity analysis
The first spatial discretization is a very simple approach which was applied during a
sensitivity analysis. Each badland is represented by one SB, one LU, one TC and one SVC.
Only the badland slopes were taken into account and the soil-vegetation component applied
represents the bare regolith on the marls.
The sensitivity analysis served to determine the influence of changes in relevant parameters
on the production of surface runoff and sediment production. Knowing the sensitivity of a
parameter allows estimating which input parameters have to be chosen carefully and which
ones may be less accurate due to low influence on the results. Furthermore, it allows
evaluating the range of uncertainty of the calculated variables. Therefore, relevant parameters
were varied within a range around the default value which is assumed to be the most realistic
one (see Table 4-5). Parameters taken into consideration were parameters from the
hydrological model as well as from the MUSLE equation. A period of one month, September
2000, was modelled. Parameters applied in this scenario were preliminary. Their derivation
will thus not be described in detail here and the results, as there are sediment production in
tonnes and runoff in m³, are not directly comparable to the other two scenarios. The results on
model performance though can be transferred to the other two studies.
46
Table 4-5: Range of values as used for the sensitivity analysis
Parameter WASA Unit Default value Derivation / source
Range over which value was varied during sensitivity analysis
Hydraulic conductivity
[mm] 512.6 Regüés et al, 2000 0.01-1000
Precipitation [mm] 50 Set arbitrarily 0-100
Manning’s roughness coefficient for overland flow
[m173/s] 0.07 Neith et al. 2002, table 19-1 mean value for no till and no residue
0-1
Peak runoff intensity - 0.9 Set arbitrarily 0-0.9
Parameters MUSLE
Erodibility factor K [(ton acre hr) / (acre ft-ton inch)]
0.21 Automatically computed by the model after Williams, 1995.
Table 5-7: Portion rill erosion of the sediment production of one TC
TC1 TC2 TC3
BL1 0.30 0.78 -
BL2 - - -
BL3 0.63 0.95 -
BL4 0.64 0.96 -
*BL2 has only one terrain component ** Lowest TC, all output is directly transferred into the river network Maximum is indicated by a red number, minimum is indicted by a green number
BL1
0.0
0.2
0.4
0.6
0.8
1.0
A B C D
routing and transport mode
sed
imen
t p
rod
uc
tio
n
TC1 TC2 TC3BL2
0.0
0.2
0.4
0.6
0.8
1.0
A B C D
routing and transport mode
sed
imen
t p
rod
uc
tio
n
BL3
0.0
0.2
0.4
0.6
0.8
1.0
A B C D
routing and transport mode
se
dim
en
t p
rod
ucti
on
BL4
0.0
0.2
0.4
0.6
0.8
1.0
A B C D
routing and transport mode
se
dim
en
t p
rod
ucti
on
Figure 5-4: Fraction of the mean annual sediment production of every TC on four badlands for different routing modes. Routing mode A = no transfer between TCs, no transport limit; B= routing between TCs, no transport limit; C= routing between TCs, transport capacity limit according to Govers (1990) and Morgan et al. 1998 (, D=routing between TCs, transport limit maximal erosion according to the MUSLE equation.
63
5.2.2. Results at the level of subbasins
5.2.2.1. Runoff generation at the level of subbasins
Table 5-8 shows the hydrological response at the level of badlands. Maximum runoff occurs
on BL3 which is the largest SB and has the largest slope (TC2) with 65283.17 m³/a. Minimum
runoff occurs on the smallest BL which is BL2 with 5175.12 m³/a. The relative values such as
runoff yield [m³/m²] and discharge coefficient [m³/m³], which is the fraction of rainfall that
becomes surface runoff, vary only little. At this level, the similarity between the badlands is
revealed. The badland slopes within BL1 and BL2 are of similar size and shape. Although
BL1 has a more differentiated structure with highland and pediment, relative runoff
production is the same as on BL2 which points out the importance of these bare areas for
runoff generation.
Table 5-9 presents minimum and maximum sediment concentration produced on each
badland. Lowest sediment concentrations are produced on BL1, highest on BL2.
Table 5-8: Runoff, runoff yield and discharge coefficient at the level of BL
Runoff [m³/a] runoff yield
[m³/m² a]
Discharge coefficient [m³/m³ a]
BL1 7351.54 0.13 0.14
BL2 5175.12 0.13 0.14
BL3 65283.17 0.08 0.09
BL4 56135.41 0.08 0.09
Table 5-9: Sediment concentration in [g/l] at the level of BL for the four routing and transport modes
BL1 BL2 BL3 BL4
Min Max Min Max Min Max Min Max
A 0.67 452.60 25.00 1561.22 1.31 231.51 2.68 331.65
B 0.83 585.92 25.00 1561.22 1.38 244.64 2.79 344.19
C 0.63 498.02 25.00 1561.22 1.25 235.79 2.56 336.91
D 0.76 458.66 25.00 1561.22 1.37 231.54 2.68 331.65
64
5.2.2.2. Sediment generation at the level of subbasins
Table 5-10 and Figure 5-7 show the mean annual sediment production, respectively sediment
yield at the level of subbasins for all four routing modes. For routing mode A, maximum
sediment production is produced on BL4 with 1387.74 t/a. Minimum sediment production
occurs on BL1 with 2193.14 t/a. The coefficient of variation for the results of the different
routing modes is as well as in case of the terrain components (see section 5.2.1.2) generally
very low except for BL1, where it amounts to 12.23%. As shown on the level of terrain
component, the TC with the highest coefficient of variation was TC3 which in case of BL1 is
more important than for BL3 or BL4 because it occupies a larger fraction of area (see Table
4-6).
The low variance shows that the difference between the routing modes is fairly low and even
disabling lateral transfer (mode A) does not lead to greater differences (see also Figure 5-7).
Table 5-12 shows the fraction of sediment that is directly routed to the river. Values are
around 90% or even higher. Not much sediment is taken into consideration for the process of
lateral distribution.
Table 5-11 contains the sediment yield for each BL. The highest sediment yield occurs on
BL2 due to its steep slopes as was shown before when describing the results of the sensitivity
analysis (see section 5.1.2). The lowest sediment yield occurs on BL3 which is the largest
subbasin but with a large fraction of inactive soils under coniferous forest which does not
contribute to the sediment production.
Figure 5-6 shows the event erosion rates for the year 2000 and the cumulative erosion in form
of the read line. This figure reveals the fact that annual sediment production is dominated by
only few intensive storm events as proposed by Gallart et al. (2005).
Table 5-13 contains the sediment production for the six individual years modelled.
Table 5-10: Mean annual sediment production [t/a] for each BL
BL1 BL2* BL3 BL4
A 2193.14 6588.89 11626.66 13877.74
B 2824.82 6588.89 12291.12 14402.41
C 2390.10 6253.25 11848.72 14101.08
D 2210.01 6588.89 11633.58 13877.97
Mean 2404.52 6504.98 11850.02 14064.80 Standard deviation 294.04 167.82 311.61 248.46 Coefficient of Variation 12.23 2.58 2.63 1.77
65
Red = maximum; green = minimum; comparing the results of mode B, C and D
Table 5-11: Mean annual sediment yield [t/m²a] for each BL
BL1 BL2* BL3 BL4
A 0.04 0.16 0.01 0.02
B 0.05 0.16 0.01 0.02
C 0.04 0.15 0.01 0.02
D 0.04 0.16 0.01 0.02
Mean 0.04 0.16 0.01 0.02
Standard deviation 0.01 4.13E-03 3.72E-04 0.00
Coefficient of Variation 12.23 2.58 2.63 1.77
Table 5-12: Portion rill erosion of the sediment production of each BL Rill erosion /
sediment output
BL1 BL2** BL3 BL4
A 99.97 - 99.99 100.00
B 78.20 - 94.64 96.36
C 91.75 - 98.17 98.41
D 99.95 - 99.98 100.00 *BL2 has only one terrain component ** lowest TC, all output is directly transferred into the river network Maximum is indicated by a red number, minimum is indicted by a green number
BL1
2193.14 2824.82 2390.10 2210.01
0
5000
10000
15000
20000
25000
30000
A B C D
routing and transport mode
Sed
imen
t p
rod
ucti
on
[t/
a]
BL4
13877.74 14402.41 14101.08 13877.97
0
5000
10000
15000
20000
25000
30000
A B C D
routing and transport mode
Sed
imen
t p
rod
ucti
on
[t/
a]
BL3
11626.66 12291.12 11848.72 11633.58
0
5000
10000
15000
20000
25000
30000
A B C D
routing and transport mode
Sed
imen
t p
rod
ucti
on
[t/
a]
BL2
6588.89 6588.89 6253.25 6588.89
0
5000
10000
15000
20000
25000
30000
A B C D
routing and transport mode
Sed
imen
t p
rod
ucti
on
[t/
a]
Figure 5-5: Mean annual sediment production [t/a] on each Badland for the four routing modes
66
0
100
200
300
400
500
Jan Feb Mar Apr May Jun Jul Aug Sep Oct Nov Dec
sed
imen
t p
rod
uc
tio
n [
t]
0
0.2
0.4
0.6
0.8
1
Figure 5-6: Event erosion rates (dots) and relative cumulative erosion (red line) on BL3 with routing mode C for climate data of the year 2000
Table 5-13: Annual erosion rates in [t] of the four badlands for the years 1997 to 2005 modelled with the time series from the climate station of Pont de Suert
c. of v. 0.00 1.52 15.39 144.10 4.63 13.67 0.00 0.06 12.14 143.01 0.00 3.68E-03 11.91 135.76
69
Table 5-17: difference in sediment production on TC2 for spatial discretization 2 and the sum of sediment production on TC2 and TC3 of spatial discretization 3 in %. Sediment production of TC2, spatial discretization 2 = 100%
BL1 BL2 BL3 BL4
A 72.16 86.59 107.58 105.60
B 111.85 118.89 147.38 144.20
C 83.84 89.37 147.37 144.19
D 111.85 118.86 147.38 144.20
mean 94.92 103.43 137.43 134.55
s.d. 20.11 17.87 19.90 19.30
c. of v. 21.19 17.28 14.48 14.34
5.3.3. Sediment production for spatial discretization 3 at the level of subbasins
Table 5-18 contains mean annual sediment production and yield at the level of subbasins for
spatial discretization 3. Although at the level of TCs, sediment generation is always higher
than in case of spatial discretization 2, total sediment output of the subbasin can be lower
using spatial discretiztion 3. Table 5-19 contains the differences between total sediment
production of the spatial discretizations in %. Results of spatial discretization 2 are set to
100%. Negative values indicate lower sediment production with spatial discretization 3.
Figure 5-7 compares the absolute sediment production for spatial discretization 2 (uni) and 3
(stripes).
Considering routing and transport mode A and B as experimental modes and only C and D as
realistic approaches to reality, in 7 out of 9 cases, spatial discretization 3 leads to higher soil
erosion in comparison to spatial discretization 2 (see Table 5-19). BL1 is little affecte by the
changes undertaken in spatial discretization 3. Sediment production on the other three
subbasins has increased by 20% though.
Table 5-18: Mean annual sediment production [t/a] at the level of subbasins for spatial discretization 3
BL1 BL2 BL3 BL4
A 1831.13 7121.43 11407.70 13751.09
B 3358.16 8613.12 15309.27 17881.52
C 2295.69 6954.17 14422.67 17246.93
D 2337.20 8612.95 14022.55 16842.22
Mean 2455.55 7825.42 13790.55 16430.44
Standard deviation 643.99 912.02 1677.09 1836.73
Coefficient of Variation [%]
26.2260 11.6546 12.1612 11.1788
70
Table 5-19: Differences in mean annual sediment production at the level of subbasin between spatial discretization 2 and 3 in %. Mean annual sediment production of spatial discretization 2 is set 100%
BL1 BL2 BL3 BL4
A -16.51 8.08 -1.88 -0.91
B 18.88 30.72 24.56 24.16
C -3.95 11.21 21.72 22.31
D 5.75 30.72 20.54 21.36
Mean 1.04 20.18 16.24 16.73
Standard deviation 14.98 12.23 12.19 11.82 Coefficient of variance [%]
1437.09 60.62 75.11 70.64
Mean (only considering mode C and D)
0.9 20.97 21.13 21.84
BL1
0
5000
10000
15000
20000
11 21 22 23
routing and transport mode
Sed
imen
t p
rod
ucti
on
[t/
a]
BL2
0
5000
10000
15000
20000
11 21 22 23
routing and transport mode
Sed
imen
t p
rod
ucti
on
[t/
a]
BL3
0
5000
10000
15000
20000
11 21 22 23
routing and transport mode
Sed
imen
t p
rod
ucti
on
[t/
a]
BL4
0
5000
10000
15000
20000
11 21 22 23
routing and transport mode
Sed
imen
t p
rod
ucti
on
[t/
a]
Figure 5-7: Mean annual sediment production at the level of badlands for spatial discretization 3. Full = spatial discretization 2; stripes = spatial discretization 3
71
5.4. Validation of the model
Data on erosion rates for the study area are rare, therefore a measuring campaign is conducted
within the SESAM project at the moment. Preliminary results of this campaign and data from
literature will be taken into consideration for the validation of erosion rates computed by the
WASA model.
As described in section 2.2, erosion rates on badlands are highly variable depending on the
method and time scale investigated, and of course the variability between different locations.
For comparison, the studies performed on the Vallcebre badlands by Clotet et al. 1986;
Balasch et al. 1988; Clotet-Perarnau et al. 1988; Gallart et al. 2002a; Regüés and Gallart, 2004
and Gallart et al, 2005 and the studies of Sirvent et al. 1997 conducted on badlands near
Lanaja (Huesca) seem to be most suitable. Both study areas are located in the Pyrenees and
thus present similar climatic conditions. In addition, the Vallcebre experimental catchment
has been set up in the early 1980s. The badlands thus have been investigated for about twenty
years. Different measurement methods have been applied and compared and the papers
published about the studies conducted there present a complete overview on processes on the
badlands at all scales. Most of the values from literature were derived for the badland slopes
explicitly which agrees with the focus of this work. Results of TC2 shall therefore be treated
predominantly in this chapter. Table 5-20 gives an overview of erosion rates as found in
literature compared with values computed with WASA. Literature values range from 120 t/ha
(Gallart et al. 2002a) up to 550 t/ha a. The modelling results for soil erosion on the badland
slopes vary between 568.36 t/ha a and 1619.78 t/ha a. For the larger badlands 3 and 4, the
results computed by WASA are more or less within the range from literature with 411.51 t/ha
a and 568.26 t/ha a, respectively. For the smaller badlands 1 and 2 WASA seems to
overestimate erosion especially when comparing them with the results derived by means of
erosion pins conducted on BL1 Table 5-20. In general though, the results are within the
magnitude of values from literature.
Reasons for the overestimation of erosion by the WASA model might be the time step of one
day which does not explicitly represent single storm events. As explained in section 2.2, the
largest part of annual soil erosion is produced during only few but intense storm events. An
hourly resolution of rainfall data could return better results.
72
Table 5-20: Comparison of results with data from literature (if not indicated, results in [t/ha a])
Vallcebre, eastern
Pyrenees
Lanaja, (Huesca, eastern
Pyrenees)
Central Ebro basin
Isábena catchment
(different authors)
Sirvent et al. 1997
Benito et al. 1992
Collector
• 258.6
• 300 – 400
Mean annual sediment yield of TC2 in t/ha a (modelling result)
BL1 BL2 BL3 BL4
A 894.78 1619.78 411.31 568.26 B 901.48 1619.78 411.58 568.27 C 894.96 1537.27 411.57 568.25 D 901.48 1619.78 411.58 568.27
mean 898.17 1599.15 411.51 568.26
Erosion pins
• 550
• 230
(Clotet_Perarnau et al. 1988)
• 123.7
• Min = 0.67
• Max = 399.09
Erosion pins applied on BL1, period of time recorder: 1 year (personal communication Till Francke)
Profilometer • 304.2 -
Suspended sediment sampler
• 120
(Gallart et al. 2002a)
-
Single rainfall event of 44 mm rainfall
• 12.5
kg/m²
Sediment yield of TC2 for a rainfall event of 45.2 mm/d; values in kg/m² (modelling result)
BL1 BL2 BL3 BL4
A 15.73 40.04 6.42 9.42 B 15.73 40.04 6.42 9.42 C 15.73 38.55 6.42 9.42 D 15.73 40.04 6.42 9.42
Sediment concentration
240 g/l (during one event)
• Max = 1561.22
Computed with WASA • Max = 2650 g/l
recorded during a storm event. (personal communication Dr. Müller)
73
6. Summary and conclusion This study aimed at estimating soil erosion rates on badland hillslopes in NE Spain by means
of a field work integrated modelling approach. The study area is located in the north eastern
Pyrenees and is characterized by a sub-humid climate with a mean annual precipitation is
767 mm/a. Rainfall distribution is characterized by high intensity storm events during spring
and summer that produce high amounts of sediment from the badland hillslopes. Longlasting
low intensity rainfalls during winter produce persistent runoff that is capable of transporting
the sediment stored in the channels.
For modelling hydrology, the hydrological model WASA (Water availability in semi-arid
areas) was applied. Although WASA was developed for application in semi-arid areas, it is
legitimate to apply it on the badland slopes of the study area for the most important process in
both climates is infiltration excess runoff during storm events. Furthermore, soil
characteristics on the badland slopes resemble the conditions of semi-arid soil. WASA is a
process-based, semi-distributed hydrological model. It accounts for interception, evaporation,
infiltration, surface and subsurface runoff, transpiration and ground water recharge as well as
lateral distribution of water between the different spatial units.
For the estimation of sediment production, WASA was combined with the empirical Modified
Universal Soil Loss Equation (MUSLE) that integrates over processes at the hillslope scale.
Besides this conceptual disagreement, a mathematical disagreement is given by the nonlinear
relationship in MUSLE between the area being considered and sediment production but the
linear routing of sediment between spatial subunits within the WASA-model. During two
weeks of field work, a survey was conducted on four exemplary badlands collecting key
geomorphological and soil hydraulic parameters on the badland slopes including size, slope,
vegetation cover, aspect, infiltration and particle size distribution. Two of the four badlands
are always similar in form and size. They can thus be compared among one another.
Model parameterization was performed based on the results of field work and data from
literature. Soil hydraulic parameters necessary for model parameterization were derived
through pedotransfer functions based on the particle size distribution of soil samples from
badland slopes.
Spatial discretization was derived by interpreting aerial photographies and GIS techniques.
A total of three spatial discretizations of increasing complexity were applied: a simple one for
the sensitivity analysis where every subbasin was represented by one terrain component
(spatial discretization 1); a detailed one which presents the best approach to the morphology
74
of the sub catchments (spatial discretization 2) and a third one which exaggerates spatial
discretization by maintaining the distribution of parameters as in spatial discretization 2 but
dividing the subbasin into a higher number of spatial subunits (spatial discretization 3).
Furthermore, four different modes of sediment transfer and transport limit were conducted
with spatial discretization 2 and 3. Routing mode A enables unlimited sediment production on
a TC but no lateral transfer. Mode B also allows unlimited sediment production but accounts
for lateral transfer from higher to lower TCs. Mode C and D both represent lateral transfer
combined with a transport limit. Mode C is limited by the transport capacity of overland flow
whereas mode D is limited by the maximum erosion possible on the corresponding area by
setting Kusle to a maximum.
The integration of the USLE approach within the hydrological model WASA has been partly
successful. The model produces consistent values at the level of terrain components and at the
level of subbasins. Spatial variability expressed by the statistical distribution of soil and land
cover through soil vegetation components is reproduced by the results for runoff and for
sediment production. Sediment yield seems to be overestimated though. Only the results of
BL1 are within the range of values from literature. The results for the other three badlands are
higher, though still within the order of magnitude of the values from literature. Preliminary
results of recent measurements of sediment yield and ground lowering performed on badland
hillslopes in the study area confirm the values form literature.
Different modes for sediment transport between terrain components produce little variance of
only in sediment production and even less in sediment yield. However, changes in the spatial
discretization lead to higher results on three out of four badlands. The variability introduced
by changes in spatial discretization is higher than those by different routing and transport
modes.
The overestimation of sediment production could derive from the modelling timestep of one
day which over represents rainfall intensity for various rainfall events occurring on one day
for they are aggregated to one large event. Furthermore, the seasonality of regolith availability
with high amounts of weathered material after the winter and decreasing values over the
course of the year has not been included in the model so far.
The effect, spatial discretization has on model output should be further investigated in order to
decide, whether or not the MUSLE is compatible to the WASA model and can be further on
applied for the modelling of soil erosion along hillslopes.
75
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8. Appendix
8.1. Appendix 1: Results of pH measurements and electric conductivity measurements for the soil samples taken within the detail study
ID #sample pH (H2O) electrical
conductivity [µs/cm]
1 G1 7.47 1119
2 G10 7.74 901
3 G2 7.65 960
4 G3 7.6 981
5 G4 7.5 n.d.
6 G5 7.84 1010
7 G6 7.64 1023
8 G7 7.5 992
9 G8 7.6 986
10 G9 7.67 911
11 GB1 7.64 1072
12 GB2 7.61 1187
13 GB3 7.44 1260
14 GB4 7.42 1253
15 GB5 7.5 1173
16 H1 7,69 959
17 H2 7.5 2320
18 H3 7.91 1303
19 H4 7.74 1451
20 H5 7.92 1984
21 R3.3 7.42 1162
22 R3.5 7.73 923
23 R1.1 7.84 1127
24 R2.2 7.7 1357
25 R2.1 7.73 1079
26 R2.4 7.87 1058
27 R1.2 7.7 1162
28 R2.3 7.75 1070
29 R3.2 7.7 920
30 R3.4 7.69 975
31 R3.6 7,84 1054
32 R1.3 7.56 1249
33 R3.1 7.48 991
34 R1.4 7.89 1360
mean value 7.66 1127.41
standard deviation 0.15 352.92
Variation coefficient 0.02 3.19
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8.2. Appendix 2: vegetation parameters needed for parameterization of the WASA module
8.3. Appendix 3: Poster about the sensitivity analysis conducted. Presented at the European Geosciences Union General Assembley 2006 in Vienna
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Erklärung Ich erkläre an Eides Statt, dass ich meine Diplomarbeit „Characterisation of badlands and modelling of soil erosion in the Isábena watershed, NE Spain“ selbständig ohne unerlaubte Hilfe angefertigt und mich dabei keinerlei anderen als der von mir ausdrücklich bezeichneten Quellen und Hilfen bedient habe. Die Diplomarbeit wurde in der jetzigen oder einer ähnlichen Form noch bei keiner anderen Hochschule eingereicht und hat noch keinen sonstigen Prüfungszwecken gedient. Potsdam,