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Acta Limnologica Brasiliensia

On-line version ISSN 2179-975X

Acta Limnol. Bras. vol.25 no.2 Rio Claro Apr./June 2013

http://dx.doi.org/10.1590/S2179-975X2013000200005 

Hydrosedimentological disequilibrium in a small, urbanized watershed

 

Desequilíbrio hidrossedimentológico numa microbacia urbanizada e de pequeno porte

 

 

Alexandre Marco da SilvaI; Alexandre Ribas dos SantosI; Rodolpho Augusto FernandesI; Rodrigo Custódio UrbanI; Romulo Martins CarvalhoI; Luiz Augusto ManfréI; Steven Frederick DurrantII

INúcleo de Automação e Tecnologias Limpas, Universidade Estadual Paulista - UNESP, Campus Sorocaba, CEP 18087-180, Sorocaba, SP, Brazil e-mail: amsilva@sorocaba.unesp.br; alexandresantos_unesp@yahoo.com.br; rodolphoff@hotmail.com; rourban@gmail.com; romulomcarvalho@gmail.com; luizmanfre@gmail.com
II
Grupo de Plasmas e Materiais, Universidade Estadual Paulista - UNESP, Campus Sorocaba, CEP 18087-180, Sorocaba, SP, Brazil e-mail: steve@sorocaba.unesp.br

 

 


ABSTRACT

AIM: In this paper we estimate the sediment yield and other related information for a small urbanized watershed, located in Sorocaba, São Paulo State. The driving forces that produce the observed scenario are presented and discussed;
METHODS: Over a year, water samples and hydrologic information concerning the river channel were collected monthly at one sampling site. In the laboratory, water samples were oven dried (80 ºC) and the total suspended solid weighed for each sample. To estimate sediment yield we used Colby's simplified method. The sediment delivery ratio (SDR) was estimated using two methods: the relief - length ratio and the bifurcation ratio;
RESULTS: The annual sediment yield estimated for the period was 1,636.1 t. The total specific sediment yield was 541.7 t.km -2.y-1. Bedload was the predominant fraction. The SDR changed between 60 and 66% according to the method employed.
CONCLUSIONS: The main driving forces of hydrosedimentological disequilibrium are the lack of riparian vegetation, the dumping of construction wastes at inadequate sites, and the launching of untreated sewage. Hence, if these three factors were controlled, a significant improvement in the environmental quality, particularly water quality, might be achieved.

Keywords: hydrosedimentology, Colby's simplified method, sediment yield, environmental impact.


RESUMO

OBJETIVO: Neste trabalho nós estimamos a produção de sedimentos para uma microbacia urbanizada e de pequeno porte, localizada em Sorocaba, Estado de São Paulo. Discutimos as principais causas que levaram ao cenário observado;
MÉTODOS: Durante um ano, amostras de água e informações hidrológicas sobre o canal do rio foram coletadas num ponto de amostragem. Em laboratório, amostras foram secas em estufa (80 ºC) e o total de sólido suspenso foi pesado para cada amostra. Para a estimativa da produção de sedimentos nós usamos o método simplificado de Colby. A Razão de Transferência de Sedimentos (RTS) foi estimada por dois métodos: a razão relevo - comprimento e a razão de bifurcação.
RESULTADOS: a produção anual de sedimento estimada para o período foi 1.636,1 toneladas. A produção específica de sedimentos foi 541.7 t.km- 2.ano -1. A carga de arraste foi a fração predominantemente produzida. RTS variou entre 60 e 66% de acordo com o método empregado.
CONCLUSÕES: As principais forças que causam o desequilíbrio hidrossedimentológico são a falta de vegetação ciliar, o despejo de resíduos de construção civil em locais inadequados e o lançamento de esgoto não tratado. Portanto, se os três principais fatores fossem controlados, uma melhoria significativa na qualidade ambiental seriam obtidos, principalmente em relação à qualidade da água.

Palavras-chave: hidrossedimentologia, método simplificado de Colby, produção de sedimentos, impacto ambiental.


 

 

1. Introduction

Urban areas are characterized by a greatly modified physical, chemical and biological environment, resulting from the construction of buildings on a large spatial scale (Taylor and Owens, 2009). Urbanization involves the growth of construction sites, which normally generate construction wastes, among them construction-related sediment (Chin, 2006). Owing to urbanization, there are also changes in the regimes of runoff and soil loss rates, which also affect the dynamics of the hydrosedimentological site.

The initial phase of urban development is characterized by a two to ten fold increase in sediment mobilization, usually caused by disruptions to the watershed, which results in deposition in the channels (Martin, 2011).

Solid waste generated at construction sites, and disposed of incorrectly, may represent an important source of sediment banks found along stretches of the river network (Ooshaksaraie et al., 2009). Some construction wastes, such as sandy materials, can be transported to water courses and dispersed in the watershed as suspended load or bedload. Increases in the concentration of coarse sand and decrease in gravel fractions have been observed in urban rivers as a result of changes in sediment yield and in the velocity of waterway (Paul and Meyer, 2001).

Many studies have demonstrated that upland land use can influence riverine ecosystems (Gergel et al., 2002). Changes in hydrological features, combined with the supplementary input of sediment from construction and also modifications in the river channel, result in geomorphological changes in stream systems (EPA, 2009). The major impact of urbanization on basin morphometry is a modification of drainage density (i.e. a decrease in sinuosity) (Paul and Meyer, 2001).

A range of other changes have also been documented. These include increases in bed material size and in drainage density, along with other chemical, biological, and ecological effects. Some of these changes may be transient, such as the increase in sediment production and sediment loads, which are part of the river landscape only until they are flushed away. But others are more lasting, especially channel enlargement or incision. In this regard, urban development does leave permanent imprints on river landscapes (Chin, 2006).

For urbanized watersheds, it is difficult to predict mathematically the sediment yield, especially if the urbanization process is spontaneous or unplanned. For small, urbanized watersheds located in subtropical regions of the Southern Hemisphere, few studies have been conducted and published regarding this theme (Scapin et al., 2007; Souza et al., 2009). The database generated in such studies may be useful to develop or improve strategies of land use and for the recuperation of degraded areas.

In South American cities, urban expansion usually occurs in a disorganized way and is not accompanied by adequate supporting infrastructure, leading to negative impacts on the environment (Poleto et al., 2009). Consequently, on this continent, there are few unpolluted streams or rivers in urban areas. Especially for São Paulo State, the most populated State in Brazil, the water quality is deteriorating (Groppo et al., 2008). Furthermore, for many countries, including Brazil, untreated sewage is still launched illegally into streams (Araujo et al., 2008), and may contribute to the sediment imbalance of the watershed, in both particulate and dissolved forms.

The observation of the effect of changes in land use on sediment mobilization in a small catchment area is an essential first step in a strategy to comprehend the problems, stress the driving forces, and collaborate on a solution of the associated problems (Porto et al., 2009). Studies addressing/the hydrosedimentological dynamic should be encouraged in these regions. Hence, the aim of this paper is to estimate the sediment yield for a small, urbanized watershed and discuss the driving forces.

 

2. Material and Methods

2.1. Study area

Sorocaba is located in the countryside of São Paulo State. It is roughly 100 km from the capital city, São Paulo (Figure 1). It has an area of 449 km2 and about 550,000 inhabitants. The Lavapés watershed falls within the boundary of Sorocaba city. The catchment area is 3.02 km2.

In the study area the average annual rainfall is 1,285 mm. Predominant soil classes are Oxisols and Ultisols (Oliveira et al., 1999). Altitude ranges from 545 to 653 m and the relief is predominantly plane (average slope 5%) (Silva, 2007).

Urban settlement is the major land cover category (71.5%) in the study area. Some areas with anthropized pastures also occur (9.6%). Natural remnant vegetation occurs in approximately 11% of the area and almost all streams have no forested riparian strips. Eight remnant forest patches (practically not riparian), of different sizes, still exist in the area (Figure 2) (Silva et al., 2011). The major part of the settlement is residential, of various social classes. Urban settlements usually reach the water courses. One consequence of this is the launching of untreated domestic sewage at many sites along the river network. There are few public, tree-lined gardens. There is little commerce and few industrial establishments. There are a few small country houses and without livestock.

2.2. Procedures

Sediment yield was estimated using Colby's simplified method (Carvalho, 1994; Vanoni, 2006; Silva and Schulz, 2007) (Equations 1, 2, 3):

Where: Qst - total sediment yield, in t day-1, Qsm - quantified solid discharge, in t day-1, Qnm - non quantified solid discharge, in t day-1, Q - stream discharge, in m3 s-1, C's - quantified concentration of sediment, in parts per million (ppm), L - channel width, in m, q'nm - not quantified solid discharge (estimated according to the width of the drainage channel), K - correction factor.

The QNM and K components were estimated using three algorithms that require information regarding flow velocity, average channel depth and sediment concentration (Carvalho, 1994; Vanoni, 2006). Use of Colby's method requires knowledge of the average channel depth, sediment concentration, average flow velocity and channel width. Such information was obtained monthly over one year in a trapezoidal, low slope, concrete surfaced and opened river channel.

The cross-section (the water depth from bank to bank) was determined at the same point used for water sampling, through a bathymetric profile. The area of the channel and the average depth were computed.

The float method (USDI, 2001) was used to determine the waterway's velocity. A float was launched from one pre-determined point upstream. When the float crossed a determined point upstream, a chronometer was started. When the float crossed a determined point 10 m downstream, the chronometer was stopped and the time recorded. This operation was executed ten times on each sampling date, always using the same upstream and downstream points. The average time was determined by computing the arithmetic average of the ten recorded values, and the average flow velocity was calculated by division of the distance (10 m) by the average time.

For the total suspended solids (TSS) at the sampling point (Figure 2) we collected water samples using new PET flasks (1L), using the vertical depth method (Carvalho, 1994). In the laboratory, the TSS was determined using the evaporation method (APHA, 1999). As required by Colby's method, the residue after evaporation was quantified in parts per million (ppm).

Channel width was determined by measuring the channel from bank to bank on the water surface at the water/sediment sampling point, using a tape.

After the determination of the sediment yield for each month, we calculated the average value of sediment yield for that period using the value of the current month and the value of the subsequent month. For example, to determine the average value for June, the values of June and July were used, and so on.

As the value was expressed in t.day -1, the average value was multiplied by the number of days of each month. For example, the average value obtained for April (average between 418.3 t day-1 and 406.9 t day-1, respectively for April and May) was 412.6 t day-1. Multiplying 412.6 t day-1 × 30 days, the resulting value for April was 12,378.0 t month-1 of sediment yielded from the Lavapés watershed. For computation of specific sediment yield we divided the annual sediment yield value by the catchment area (Haan et al., 1994).

The sediment delivery ratio (SDR), expressed as the percent of gross soil erosion by water that is delivered to a particular point in the drainage system (Da Ouyang, 1997), was estimated using two approaches: (1) the relief - length ratio technique (Equation 4 and Figure 3) (Carvalho, 1994; Haan et al., 1994); (2) the bifurcation ratio method (Equation 5) (Roehl, 1962; Carvalho, 1994; Haan et al., 1994).

 

 

Furthermore, a map showing the distance from the river network was elaborated using a GIS package and employing a 1:50,000 Digital Elevation Model of the study area.

Where: RC - Relief - channel length ratio (dimensionless) - to be plotted in Figure 3, D.A. - Difference of the elevations in the watershed divide and outlet (m), C - Length of main river channel of the watershed (m).

Where: DR - SDR (%), W - watershed area (km2), R - relief - channel length ratio, B - bifurcation ratio (average value).

Considering that (1) measuring the electrical conductivity (EC) of the water is a suitable method to estimate the concentration of salts present (Ikeda et al., 1991) and to evaluate the degree of pollution, and (2) that the EC and concentration of total dissolved solids are in general closely associated (Das et al., 2006), on the same day with the hydrosedimentometrical samplings, EC was measured in situ using a previously calibrated Akso PCS35 EC meter.

 

3. Results and Discussion

The annual sediment yield was 1,636.1 t. Not surprisingly, the total load was significantly smaller during the low water period than during the high water period (Silva and Schulz, 2007; Filizola and Guyot, 2009). December to January presented the greatest value, whereas June to July presented the lowest (Figure 4).

 

 

The specific sediment yield was 541.7 t.km -2.y-1. Such a value is greater than the 422 t.km -2.y-1 found by Machado and Vettorazzi (2003) in an Brazilian watershed (59.7 km2) located in Piracicaba (100 km from Sorocaba) and it is close to values estimated by Haan et al. (1994) for various small watersheds scattered throughout the world.

The average monthly value for suspended load was 33.5 t, for bedload it was 102.9 t. Bedload was the predominant fraction of transported sediment throughout the period of study (Figure 5).

 

 

Owing to such results and others discussed below, we decided to carry out field work along the entire river network. In these trips neither expressive linear erosion features nor landslides were observed. These erosion features normally represent an important source of sediments (Nelson and Booth, 2002).

Some unpaved streets, however, of which some were located close to river channels, were observed. Such features might be a possible source of sediment in medium to heavy rainfall events (sheetwash on road surfaces (Barton, 2002)), and indicate that sheet erosion seems to have much more influence on the sediment yield than linear erosion. In some catchments, sheet and rill erosion could dominate the sediment supply, whereas in others, channel erosion or gully erosion represents the primary source (Walling, 2005).

Some vacant lots were also observed in the study area (photo "C" of Figure 6). We observed construction wastes in some lots (photo "F" of Figure 6). Deforestation caused by urban expansion was not detected, but in dry months it is possible to observe some areas covered with burnt and sparse vegetation. There are many dwellings that practically reach the river channels, and are thus areas hydrologically threatened (photos "B", "E", Figure 6).

Increased coarse sediment supply does not raise chemical concerns, but can cause channel aggradations, resulting in reduced flow capacity that might lead to flooding or navigational problems and channel instability (Nelson and Booth, 2002; Allan, 2004). This is a typical scenario observed in the study area and perhaps the main concern raised by this study. Photo "E" of Figure 6 depicts a stretch of silted river.

Some parts of the river network have experienced enlargement of the channels and invasion by amphibian vegetal species, contributing to the siltation process (see photos of Figure 6). We observed that the factors affecting the enlargement of streams are: (1) streambank erosion occurring mainly in "U" shaped channel stretches due the nonexistence of forest riparian vegetation (photo "D" of Figure 6); (2) water pollution that stimulates an increase in amphibian macrophytes, favoring the siltation of some parts of the river network.

The scenario described does not occur uniformly along the entire catchment, in agreement with Booth (1990), who affirms that "whereas some channels expand gradually to accommodate a new, higher magnitude flow regime, other channels incise rapidly into their substrate, evacuating a proportionally much larger channel form whose capacity bear little relationship to the flows, either past or present, that have occurred".

We also observed that in many stretches the channels were straightened. The current drainage density (Dd) value is 1.89 km of river.km -2. This value was certainly greater before urbanization (some decades ago), but due to the straightening process, the Dd value has diminished. This contributes to the increase in the flow in rainy periods, and this encourages the bedload of sediment at least in part of the watershed (Vanoni, 2006).

On many parts of the roads and also in many parts of river network (bed or banks) we observed coarse sand (photo "A", Figure 6) and fragments of tiles, bricks and other construction wastes that certainly are not materials autochthonous from the study area. In normal conditions, according to particle size, sediment tends to be deposited along a gradient down a river (Haan et al., 1994; Vanoni, 2006). But this does not occur in the study site, characterizing hydrosedimentological disequilibrium. The deposition of coarse - very coarse sediment downstream reduces roughness in the river bed and banks (Gregory, 2006).

The elevation range of the study area is 108 m, and the length of the main river channel is 2,855 m. Using these values in the relief-length relationship, a value of 0.037 was obtained. Plotting the resulting values in Figure 3, the SDR is estimated to be 60.0%. Using Equation 5, the estimated value is 66.0%. Taking into account the catchment area of the studied watershed and the SDR values, we consider that in the studied area the SDR is extremely high (Carvalho, 1994). We can see that the shape of the catchment area is not perfectly circular. Consequently, there are different distance gradients between upland points where soil particles may be detached and points in the river network where the sediment reaches the channel (Figure 7).

 

 

River discharge values did not present any significant correlation with the other parameters. On the other hand, a significant correlation value was noted between EC and TSS (r2=0.7, significant =1%), that presented seasonal similarity (Figure 8). The correlation value between the TSS and mineral fraction was 0.6 (significant =5%), whereas between TSS and organic fraction it was 0.7 (significant = 1%). The predominant fraction was mineral (average annual value 70%). An exception was July, which presented an organic value of 73.4% (Figure 9).

 

 

The EC presented an average value of 300.1 µS.cm -1 and ranged from 89.8 to 408.0 µS.cm -1. On only two occasions were the values below 200 µS.cm -1. According to Figure 2, the study area has 69.5% of urbanized area. Comparatively, for a rural, small watershed located in São Carlos (220 km from study area), covered only with remnant vegetation patches and pasture, Primavesi et al. (2002) found values ranging from 6.1 to 25.6 µS.cm -1. Ometto et al. (2000) studying two small watersheds in the Piracicaba region, observed values for EC ranging from 55.5 to 81.6 µS.cm -1 for the Cabras watershed (1.5% covered by urban settlements) and ranging from 81.6 to 272.8 µS.cm -1 for the Pisca watershed (10% covered by urban settlements). Ometto et al. (2000) stress that in such watersheds, domestic sewage is launched into the rivers and the impact of the urban areas is directly proportional to their size.

Photo "B" q µS.cm -1 for the Sorocaba River (the river into the which Lavapes stream flows, Figure 10). These values were lower than the ones observed for Lavapes stream. Therefore, we believe that Lavapés is a considerable source of ions that flow into the Sorocaba River and, in the current state of conservation, the Lavapés stream contributes to deterioration of the water quality of the Sorocaba River.

 

 

Considering that gradients of anthropogenic land use are frequently superimposed on a gradient of physical environmental features, such as geological formation, soil type, topography, and others (Allan, 2004), we can summarize the anthropogenic driving forces that promote the hydrosedimentological imbalance of the region (Table 1). We created Table 1 to emphasize the threats, and comment that if controlled, an expressive improvement in the local environmental quality of the study area might be achieved.

The rapidly expanding investigation of streams in the context of their catchments and landscapes clearly indicates that stream ecosystems are strongly affected by human actions across spatial scales (Allan, 2004). The studied area represents 0.7% of Sorocaba City. It is a small catchment, but influences many people who live in Sorocaba. Population size influences material importation, transformation and waste generation, but these aspects of urban metabolism are also dependent upon biophysical factors, urban forms and social factors (Kaye et al., 2006).

Historic conditions in many streams can greatly be modified as increasing urban runoff transforms intermittent and ephemeral drainages into perennial streams with elevated flood discharges. The urbanization-induced hydrological changes that have altered stream and riparian vegetation communities also probably affect the native wildlife species associated with them (White and Greer, 2006).

Similarly reported by such authors for a temperate catchment, the scenario certainly also occurs in other catchments of Sorocaba, but none have yet been studied and certainly there is no detailed knowledge sufficient for a solution to the related problems. This study suggests some actions and encourages futures studies in others parts of the city.

 

4. Conclusions

The annual sediment yield estimated for the period of the experiment was 1,636.1 t. The specific sediment yield was 541.7 t.km -2.y-1. Bedload is the predominant fraction and we conclude that it is an important threat to the study area, whose driving forces, which cause this problem, should be controlled. Geomorphic changes to stream channel morphology were observed and clearly have been influencing the hydrosedimentological dynamic of the study area.

We affirm that the increase in urbanization of the study area has resulted in a hydrosedimentological disequilibrium caused by the inexistence of riparian vegetation, the dumping of construction wastes, and the inadequate disposal of sewage. We stress that if the main degrading factors were controlled, an expressive improvement of the environmental quality might be achieved. The main activities should focus on inspection to avoid (or eliminate) degrading activities and for reconstruction of natural or semi-natural environments in severely damaged areas.

 

Acknowledgements

We are grateful to the Brazilian agencies FAPESP and FUNDUNESP for financial support.

 

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Received: 14 August 2011
Accepted: 14 August 2013

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