Original paper

 

Bottom topography, recent sedimentation and water volume of the Cerro Prieto Dam, NE Mexico

 

Vsevolod Yutsis^1,2*, Konstantin Krivosheya¹, Oleg Levchenko³, Jens Lowag⁴, Héctor de León Gómez⁵ and Antonio Tamez Ponce⁶

 

¹ Universidad Autónoma de Nuevo León, Facultad de Ciencias de la Tierra. Carretera a Cerro Prieto km 8 Linares, 67700, N.L., México. *Corresponding author: vyutsis@hotmail.com

² V. Yutsis. Instituto Potosino de Investigación Científica y Tecnológica, A.C. División de Geociencias Aplicadas. Camino a la Presa San José 2055 Lomas 4ª. Sección, 78216 San Luis Potosí, S.L.P., México.

³ P.P. Shirshov Institute of Oceanology, Russian Academy of Science, 36 Nahimovsky prospect. Moscow, 117997, Russia.

⁴ Innomar Technologie GmbH, Schutower Ringstrase 4, 18069, Rostock, Germany.

⁵ Universidad Autónoma de Nuevo León, Facultad de Ingeniería Civil. Avenida Universidad s/n Cd. Universitaria, San Nicolás de los Garza, 66451, Nuevo León, México.

⁶ Posgrado de la Facultad de Ciencias de la Tierra, Universidad Autónoma de Nuevo León. Carretera a Cerro Prieto km 8 Linares, 67700, N.L., Mexico.

 

Received: July 07, 2012.
Accepted: April 16, 2013.
Published on line: December 11, 2013.

 

Resumen

La presa Cerro Prieto, relativamente una pequeña reserva de agua en el noreste de México, es uno de los principales recursos de agua potable para Monterrey, ciudad con una población cerca de cuatro millones de habitantes. Se llevó a cabo un estudio de sísmica de alta resolución en esta reserva de agua con un equipo SES-2000 que utiliza un efecto acústico paramétrico no lineal. La interpretación de los datos de acústica de alta resolución muestra que el espesor de los sedimentos recientes alcanza 3.5-4.0 m debido a la sedimentación del embalse. Esto demuestra una alta velocidad de sedimentación reciente (de 1-2 hasta 14 cm por año). Con base a los resultados de este estudio, se ha preparado un mapa batimétrico y un modelo de espesores de sedimentos. Se reveló una diferencia significativa (5-12%) entre el valor de la capacidad de volumen calculado por la Comisión Nacional del Agua (CNA) y los resultados acústicos. La diferencia entre dichos datos indica pérdidas de almacenamiento de 12-17 hasta 30 millones de metros cúbicos. Los resultados obtenidos de un estudio como éste, son útiles para mejorar un sistema de gestión de los recursos hídricos.

Palabras clave: acústica no lineal, NE de México, reserva de agua, topografía del fondo, capacidad de agua, sedimentación reciente.

 

Abstract

The Cerro Prieto dam, a relatively small water reservoir in NE Mexico, is one of the main resources of potable water for Monterrey, a city with a population of about four million inhabitants. A high resolution seismic study using non-linear parametric sub-bottom echo-sounder SES-2000 was carried out in this water reservoir. High resolution acoustic data interpretation shows that the thickness of recent sediments due to siltation of the reservoir reaches 3.5-4.0 m. It shows a high recent sedimentation rate (1-2 up to 14 cm/year). Based on the echo-sounder data, the first bathymetric map and a digital model of recent sediment thickness were designed. A significant (5-12%) difference between the volume capacity value used by National Commission of Water (CNA) and acoustic survey results was revealed. Differences between the CNA and acoustic data indicate storage losses from 12-17 up to 30 million cubic meters. The results obtained through study such as this one, could be useful to improve a water resources management.

Key words: non-linear acoustic method, NE Mexico, water reservoir, bottom topography, water capacity, recent sedimentation.

 

Introduction

The role of bathymetry and recent sedimentation in water reservoir management is very important (Bowen, 1982), especially in the case of semi-arid countries (Annandale, 1987; Martínez et al., 2010; Schleiss, 2008). Due to its physiography, the State of Nuevo León in North-East Mexico is characterized by semi-arid climate, undeveloped drainage, mostly low precipitation, and high evapotranspiration rates, as well as rapid demographic growth. Due to these characteristics, domestic water supply shortages have been occurring since 1979, making this a major problem for the state government. Monterrey, the most important industrialized city in the state with a population of about four million inhabitants (INEGI, 2009), faces a serious water supply scarcity (Navár, 2001; Navár, 2004). At present, ground water sources (Campo de Pozos de Mina, Sistema Santa Catarina, Sistema Santiago I, and Campo de Pozos Monterrey) and superficial waters (La Boca, Cerro Prieto and El Cuchillo dams) form the main water supply. The overall water supply demand for Monterrey city is calculated as a daily amount of 370 liters per capita, with an additional 17 m³/s required for domestic, industrial and city usage. Yet the actual supply is about 11 m³/s, i.e. city demand is short of about 6 m³/s (De León-Gómez, 1993; De León-Gómez et al., 2004; De León-Gómez et al., 2006).

The Cerro Prieto dam was built in a two years period (1980-1982) by the Secretaria de Agricultura y Recursos Hidráulicos (SARH) now known as National Commission of Water (Comision Nacional del Agua, CNA). The dam is located 130 km southeast of Monterrey and 20 km northeast of Linares. Cerro Prieto dam belongs to the regional system of water supply known as Linares-Monterrey. The storage capacity of the dam was calculated as almost 400 million m3 (De León-Gómez, 1993). The main objectives for the construction of this dam were to supply 4.1 m³/s of water for city of Monterrey, to irrigate 673 hectares, and to control peak discharge during hurricane seasons. The hydrological basin has an area of 1708 km² and is influenced by the southeastern part of the Monterrey Salient (Sierra Madre Oriental) and the northeastern part by the "Planicie Costera del Golfo Norte" (Coastal Plane, see Figure 1). The main sources are the Pablillo and Camacho rivers.

Concerns exist about the future of many Mexican reservoirs which are prone to soil erosion and subsequent siltation produce losses in storage capacity. Additionally, the number of studies of these problems is poor. Lake Cerro Prieto shares this problem with most impoundments in Nuevo León State.

The first step of the integral geological study of the Cerro Prieto water reservoir was geophysical prospecting including gravity, magnetic, electrical and shallow (onshore) seismic methods (Izaguirre Valdez, 2008; Yutsis et al., 2009). It was oriented to recognition of sedimentary and upper basement structures of the Cerro Prieto area. As a follow-up to the earlier study, new research has been focused on the question whether recent sediments of artificial basins are significant and whether the volume of recent sediments affects the reservoir volume? If so, what are the consequences for water supply?

The objective of this study is to conduct a detailed bathymetric and geo-acoustic survey of the artificial reservoir in order to: (1) obtain an accurate map of Lake Bathymetry (depth) and reservoir volume values, and (2) study the distribution, thickness and volume of recent sediments in the reservoir.

Various ways could be used for this purpose. They are time-lapse bathymetry survey or some traditional tools like coring (Helsel and Hirsch, 2002; Anderson, 1986; Jones, 1999) and/or geophysical studies (Bièvre, 2005; Kirsh, 2006; Mainali, 2007; Rubin et al., 2006; Sharma, 2002). The present study applies a geo-acoustic tool (a non-linear parametric sub-bottom echo-sounder) combined with typical techniques of geophysical survey. It is shown that high resolution seismic profiling is useful to quantify sedimentation rates and reservoir storage loss effectively. Especially it should be useful for initial studies of reservoirs where no previous bathymetry or bottom topography maps exist.

 

Data collection

Sedimentation of artificial reservoirs tends to be low. For example, a sedimentation rate of 1-2 cm/year causes a total accumulation of about 20-40 cm for 20 years of the reservoir operation. In order to be effective, new techniques for the estimation of sedimentation (such as acoustic equipment) should be able to provide a high vertical resolution.

 

Non-linear parametric acoustics equipment

In this study, we used the SES-2000 parametric (non-linear) dual frequency echo-sounder. The instrument simultaneously transmits two signals of slightly different high frequencies; their interaction creates a new low frequency signal. It has a large bandwidth and a short signal length, which allows good use in very shallow water and results a high (~15 - 20 cm) vertical resolution (Missiaen et al., 2008) at acceptable sub-bottom penetration up to 10 m or more. Some favorable near sub-bottom seismic and geological conditions permit to achieve a vertical resolution up to 10 cm.

Parametric (non-linear) sound generation allows designing acoustical systems with small transducer dimensions and narrow sound beams at low frequencies. An Innomar SES-2000 parametric transducer has an active area of 20 by 20 cm and provides a beam width of less than four degrees (at 3dB), valid for all adjustable low frequencies between 5kHz and 15 kHz (Wunderlich and Müller, 2003). The transmit directivity of the parametric sound beam does not show any significant side lobe characteristic, which reduces ambiguities during the interpretation of individual reflectors. Short transmit signals of single sinusoidal cycles without any ringing and high ping rates of up to 50 pings per second are further advantages. They contribute to a high spatial resolution of this acoustical system and permit to apply it in a shallow basin.

Innomar's software tool ISE provides near real-time processing of the collected SES data. The operation procedure can be tuned on-line. A value of the sound velocity in water is used to convert sound travel time to the depth. The depth values are screened online.

Some advantage of the SES-2000 parametric (non-linear) dual frequency echo-sounder is the survey of small water reservoirs, which often requires the collection of sub-bottom data from small boats in water depths of down to one meter and to resolve thin layers of recent sedimentation due to damming. Furthermore, the determination of near surface structures, e.g. shallow fault zones, is of interest at the same time and can be achieved with the application of such a mobile parametric profiler system (Wunderlich and Wendt, 2001; Vasudavan et al., 2007; Wunderlich, 2007).

 

Data acquisition methodology

The aquatic survey of the Cerro Prieto water reservoir was conducted on-board of a small motor boat (5 m). The SES-2000 transducer was mounted on the front side of the boat 0.75 m down from the water level using a light metal pipe, and all electronic equipment was installed on the deck. Accurate positioning of the boat was reached using Global Positioning System (GPS). Average speed was 8-10 km/h.

A total of 32 acoustic profiles have been acquired. The track map is shown at the Figure 1. Line separation is about 300 m. Twenty six profiles were made at near right angles to the axis of the basin. Five lines were oriented along the river Pablillo valley and finally one profile was made circular, skirting the shoreline. Some lines have been repeated to provide the quality control. Difference in depth measurement for different data sets does not exceed ±2-5 cm.

A sound velocity profile in the lake was not taken. Acoustic depth measurements were calibrated by direct depth measurements (at some points) at different parts of the lake.

 

Results and discussion

As it is mentioned above the water depth and sediment layer thickness are calculated from sound pulse travel times. The water sound velocity mean value of 1450 m/s was used (Kinsler et al., 1991). Velocity uncertainty is evaluated of 0.5-1%. Calibration of acoustic bottom depth for some points allows us to obtain the depth accuracy ±10-20 cm. This is limited mainly by weather conditions. The same velocity value was used for sub-bottom sediments. It is supposed velocity uncertainty of 3-4%. For mean value of sediment thickness 50 cm the velocity uncertainty of 4% corresponds to ±2 cm of thickness uncertainty. Uncertainties of sediment velocity of 3-4% for 3-4 m sediment layer thickness could cause ±12-15 cm variations.

Integral model based on CNA data of water balance and lake surface area allows evaluating storage loss due to uncertainties of water sound velocity (maximum ±8 x10⁶ m³ for 4% and ±2 x10⁶ m³ for 1 %). For this study estimated sound velocity uncertainty is about 0.5%, which corresponds to maximum volume loss ± (1-1.5) x 10⁶ m³. The value ±5 cm of sediment thickness uncertainty corresponds to ± (0.6-1.4) x10⁶ m³ of uncertainty of sediment volume.

Acoustical reflectors on the depth sections have been picked and digitized. Digital data sets of the bottom depth and the depth of the base of recent sediments (the acoustic basement depth) were used to generate the bathymetric model, the model of sediment thickness and to calculate water storage volume.

 

Bathymetry and bottom morphology

Acoustical sections provide detailed information of bottom morphology and sub-bottom sediments. Figure 2 and Figure 3 show typical echo-plot samples. Figure 2 shows a fragment of the circular profile, which is located in the western part of the lake. This is a relatively shallow part of the water reservoir. The depth of the bottom is not more than 4-6 meters. In general, the bottom is relatively smooth (Figure 2c), but in places the detailed topography is somewhat complex and irregular (Figures 2a, 2b).

Figure 3 shows an acoustic line, which is situated in the eastern deep part of the Cerro Prieto Lake crossing the ancient river Pablillo valley in NW-SE direction. The water depth here is calculated as 18-24 m (Figure 3a). In this area the bottom is mainly smooth. A small trough extending in WSW-ENE direction is shown at Figure 3b. The trough bottom depth is more than 28 m, and width ranges 40-60 m (Figure 3b).

It is observed significant difference (up to 5-7 m) between acoustical depths and a previous topographic map. It is supposed that the original topography (land surface) has been changed and the river Pablillo valley has been deepened during construction of the dam (De León, 1993, Figure 4). The previous topographic map by Instituto Nacional de Estadística y Geografía (INEGI) (INEGI, 1980) demonstrates the smoothed topography features of the area. They are the undulating surface of the river Pablillo valley at the elevation between 252-310 m (Figure 6). The bathymetric survey with the SES-2000 parametric echo-sounder has resulted in a modification of some important aspects of this map and, also, in the construction of the first bathymetric map of the Cerro Prieto water reservoir (Figure 7).

The irregular bottom topography of the reservoir is revealed. Taking into account that the water surface was at the altitude of 282 m above sea level during acoustic study, the depth of the reservoir ranges from 0.0-1.0 to 28 m (Figures 6, 7). Figure 7 shows the general topography of the Cerro Prieto Lake bottom based on survey results in combination (co-kriging) with the Digital Elevation Model (The Consortium for Spatial Information, 1980).

It is possible to recognize two different areas in the lake basin. The western shallow-water area is largely occupied by a flat bottom (depth 0.5-10 m), except for a bottom elevation trending in the northeastern direction. The elevation has a relative height of about 2-3 m from the bottom of the lake. The western area is divided into NE and SW regions. To the southeast of the elevation, a smooth floor tends to be gently inclined from its peripheral parts towards the east. The North of the western area is characterized by relatively low relief (up to -12 -13 m) and tends to be deeper toward southeast (Figure 7).

A chain of islands is located in the central part of the water reservoir. The large island called the Cerro Prieto Island, and rises up to 25-30 m above the surrounding bottom floor near the south coast (Figures 7). Another one situated to the west-northwest and has a single pointed peak. An area of four small islands occurs to the north of the Cerro Prieto Island, topographic high which divides the water reservoir into western and eastern areas.

The eastern deep-water area is situated to the northeast of the Cerro Prieto Island (Figure 7). It is characterized by irregular topography. The bottom depth is generally more than 15-20 m and attains a maximum depth of approximately 28-30 m (Figure 7). So the deepest part of this area occupies the easternmost region which is situated near the dam and artificial dykes. At the southeastern part of the lake the basin bottom lies at a depth of between 22-24 m, interrupted by small bottom hills in some places.

 

Recent sedimentation

Recent sediments of the Cerro Prieto water reservoir have been deposited on the floor of river Pablillo valley for about 28 years. In case of recent non-consolidated sediments (case of Cerro Prieto dam) we have some kind of pulp, or suspension of fine particles (silt, mud), and it is supposed that usually the silt has a velocity the same (or slightly less) as the water.

The interpretation of the SES profile at the western shallow-water area (Figure 2) shows two reflectors. We identify a strong sub-bottom reflector distributed almost throughout the whole lake as the most likely base of recent sediments. We also identify a few hypothetical bright seismic sub-bottom facies, which we attribute to recent "lake" sediments, quaternary river "pre-lake" sediments (alluvium), and cretaceous bed rocks. The uniform thinness of the upper acoustic unit for the whole basin is more relevant for new "lake" sediments than for alluvium. The quaternary river sediment thickness demonstrates essential variability around the water reservoir. In the western part of the lake the thickness of this layer is usually less than 1 meter. Most of the profiles here show a sediment thickness of 30-50 cm or, even, an absence of sediments. At the eastern deep part of the Cerro Prieto Lake thickness of recent sediments is 1.0 – 1.5 m (Figures 3c, 3d). The maximum thickness values are from 3.5 up to 4.0 m (Figures 5, 8). It may be partly caused by a sub-water slumping process or redistribution of sediments (Figure 5). And it means the maximum sedimentation rate could be over 14 cm/year.

Recent sediment thicknesses obtained from the interpretation of non-linear acoustic have been mapped (Figure 8). Sediment thickness within the lake basin varies from zero to over 3.5 m. There are five centers of sediment accumulation localized in the eastern deep area. The greatest thicknesses occur in narrow bottom valleys (troughs) in the central and eastern parts of the lake (Figures 7, 8).

The sediments in the basin are generally confined to the southeastern part of the lake. The western area is relatively shallow and the sediments are thin (0-0.5 m). It means that average rate of the siltation is up to 1-2 cm/year.

The river Pablillo is the main source of water and sediments for the basin. So, it seems rather strange that the western part of the lake near river mouth does not show a large amount of sediments. We hypothesize that sediments are mainly fine grained (silt), deposited slowly and distributed by water currents uniformly through the basin.

The total volume of this accumulated material estimated by the acoustic data is approximately 8.8±0.5 million cubic meters. It is possible to suppose that some recent sedimentary layers (bodies) are not reflected on the acoustic records. This means that the volume of the acoustically visible sediments could be less than the real (total) volume of sediments.

 

Water storage

Analysis of the storage volume was conducted using three data sets: the Digital Elevation Model of Cerro Prieto and surrounding area (The Consortium for Spatial Information, 1980), a register of the water balance of Cerro Prieto dam, and new data of the high resolution acoustic survey.

According to CNA reports the maximum water storage of the Cerro Prieto water reservoir is 393 million of cubic meters, which corresponds to a water level of 285 meters above sea level (a.s.l.) (see Table 1, volume CNA). However, this level was reached only three times after the dam's construction. Hurricanes Gilbert (1988), Keith (2000), and Emily (2005) contributed to reach the full capacity storage of the dam.

Table 1 shows summary data of the water storage of the lake and the surface area of the reservoir for different water levels, calculated according to the Digital Elevation Model (DEM) and SES echo-sounding data. The procedure comprises a standard hydrological modeling (implemented in Arc/Info) that is a cell-based modeling of water depth and storage volumes (Stout et al., 1985). In both procedures the Digital Elevation Model for Linares and surrounding areas from INEGI (Instituto Nacional de Estadística, Geografía, e Informática) was used. Grid node spacing was 30 x 30 m.

The volume capacity values (Figure 9) derived from the analysis of the bathymetric map (Figure 7) indicate a predicted total storage capacity of 360 million m3 (Table 1), whereas the storage capacity generated from DEM shows only 279 million m3. This discrepancy could be explained by the fact that the Digital Elevation Model was developed in the early 80-ies before the dam construction and excavations of the basin material as reported by De León (1993) (Figure 4).

The volume of water, mentioned in the report of CNA, is approximately (12-17) ±2 million m³ larger than the amount calculated from the SES data for operation levels 280-275 meters respectively (Table1). This can be explained by recent sedimentation.

There is a difference between the loss in storage capacity and calculated sediment volume (8.8 ± 2 million cubic meters). It is possible supposed that calculated sediments could be underestimated. Nevertheless, the observed difference in calculated sediment volume (8.8 million m³) and loss in observed storage capacity (12-17 million m3) changes the average sedimentation rate a little (from 1.5 up to 2 cm/year).

The trend line of water volume (simulation) shows that sediment accumulation between 1982 and 2009 in the Cerro Prieto Lake could result a loss up to 30 million m3 of storage capacity (Table 1, Figure 9) for maximum operation level (285 m a.s.l.). And 17 million m3 for low operational level (275 m) is more critical. It corresponds to storage loss 19% of total volume or 11-12 days water supply (four million inhabitants x 370 l/day).

 

Conclusions

This study discusses the advantage of geophysical data to evaluate the current state of water reservoir (distribution of recent sediments and real storage capacity).

Analysis of the non-linear echo-sounding data provides the volume of the reservoir at different levels of water table and the volume of sediments as well as distribution of the sediments through the basin.

A high rate of recent sedimentation (1-2 up to 14 cm/year) at the artificial water reservoir is revealed. Interpretation of the SES echo-sounding data shows that the thickness of sediments due to siltation of the reservoir reaches 2.5-4.0 m. The total volume of this accumulated material estimated by the acoustic data is evaluated about 9 million cubic meters.

The volume of water, calculated from the acoustic data for common operating levels is approximately 12-17 million cubic meters smaller than the values of operational management data. This is about 5-12 % of total storage capacity. A significant reduction in the size and volume of the reservoir is obvious. This factor could have been taken into account in the calculations of the volume of water for this reservoir.

 

Acknowledgements

The authors would like to thank Universidad Autónoma de Nuevo León (UANL), Mexico, for funding support of the project PAICYT CT-1705-07 and Innomar Technologie GmbH, Germany, who kindly provided the SES-2000 compact equipment. We are indebted to Pedro Garza of National Commission of Water (Rio Bravo Division, Monterrey) for providing access to water balance data. Authors thank Dirk Masuch Oesterreich (UANL) for his assessment of GIS calculations. We also would like to thank Dr. John M. Sharp, Jr. (The University of Texas at Austin), Dr. Vadim Galkine (Canada) and Dr. Wouter Buytaert (Imperial College, Great Britain) for their constructive comments and suggestions, which helped to improve this paper. Comments and suggestions from two anonymous reviewers and the editor are greatly appreciated.

 

Bibliography

Anderson R.N., 1986, Marine geology. Wiley & Son, 328 pp.         [ Links ]

Annandale G.W., 1987, Reservoir sedimentation. Elsevier, Amsterdam, 221 pp.         [ Links ]

Bièvre G., Norgeot Ch., 2005, On the use of geophysical methods for characterization of earth dams: A case study on the Canal du Centre (France). Bulletin des Laboratoires des Ponts et Chaussèes, 254, 85-107.         [ Links ]

Bowen R., 1982, Surface water. Wiley Interscience Publ., New York & Toronto, 290 pp.         [ Links ]

Instituto Nacional de Estadística y Geografía (INEGI), 2009, Anuario estadístico de los Estados Unidos Mexicanos, http://www.inegi.org.mx. Cited 20 Sept 2010        [ Links ]

The Consortium for Spatial Information, 1980, Digital Elevation Model. http://www.csi.cgiar.org. Cited 12 Apr 2007.         [ Links ]

De la Garza-González S. I., 2000, Estudio geológico/hidrogeológico en la región citrícola (Linares-Hualahuises) Nuevo León, México. Tesis de licenciatura. Facultad de Ciencias de la Tierra, UANL, 131 pp.         [ Links ]

De León-Gómez, H., 1993, Die Unterlaufigkeit der Talsperre José López Portillo/Cerro Prieto auf einer Kalkstein-Mergelstein-Wechselfolge bei Linares, Nuevo León, Mexiko. Mitteilungen zur Ingenieurgeologie und Hydrogeologie 53, Aachen, 181 pp.         [ Links ]

De León-Gómez H., Schetelig K., Werner J., Azzam R., Masuch D., Medina-Barrera F., Rangel-Rodríguez M. M., Navarro-De León I., Salinas-Ramírez J. O., 1998, Water supply limit in the northeast Mexico, objective and scope. (SIREYES/95/053).- Zbl. Geol. Paläont., Stuttgart; Teil I, H 3-6, 511-518.         [ Links ]

De León-Gómez H., Medina Barrera F., Lizárraga Mendiola L., 2006, Elaboración de la matriz de geoindicadores ambientales en la presa José López Portillo (Cerro Prieto), fuente superficial de abastecimiento de agua potable de Monterrey, N. L., México. Ciencia UANL., IX (1), 65-72.         [ Links ]

Helsel D.R., Hirsch R.M., 2002. Statistical Methods in Water Resources. In: Techniques of Water-Resources Investigations Book 4, Hydrologic Analysis and Interpretation, U.S. Geological Survey, Chapter A3. U.S. Geological Survey, 522 pp, http://pubs.usgs.gov/twri/twri4a3/, accessed March 2011.         [ Links ]

Izaguirre Valdez F.M., 2008, Estudio hidrogeofísico de la presa José López Portillo (Cerro Prieto), Noreste de México. Tésis de licenciatura, Universidad Autónoma de Nuevo León, Facultad de Ciencias de la Tierra, 192 pp.         [ Links ]

Jones E.J.W., 2004, Marine geophysics. Wiley & Son, 466 pp.         [ Links ]

Kinsler L.E., Frey A.R., Coppens A.B., Sanders J.V., 1991, Fundamentals of acoustics, Wiley and Son, 518 pp.         [ Links ]

Kirsch R., 2006, Groundwater geophysics. A tool for hydrogeology. Springer, Heidelberg, 493 pp.         [ Links ]

Mainali G., 2007, Monitoring of Tailings Dams with Geophysical Methods. Division of Ore Geology and Applied Geophysics, Luleå University of Technology, SE-97187 Luleå, Sweden, 93 pp.         [ Links ]

Marín-Córdova S., Campos-Enríquez O., Herrera-Moro-Castillo M., 2004, Geofísica Internacional, 43, 3, 435-443.         [ Links ]

Martinez S.E., Escolero O., Wolf L., 2010, Total Urban Water Cycle Models in Semiarid Environments — Quantitative Scenario Analysis at the Area of San Luis Potosi, Mexico. Water Resources Management, DOI 10.1007/s11269-010-9697-6.         [ Links ]

Missiaen T., Slob E., Donselaar M.E., 2008, Comparing different shallow geophysical methods in a tidal estuary, Verdronken Land van Saeftinge, Western Scheldt, the Netherlands. Netherlands Journal of Geosciences — Geologie en Mijnbouw, 87, 2, 151–164.         [ Links ]

Navár J., 2001, Water supply and demand scenarios in the San Juan watershed. Geofísica Internacional, 40, 2, 121-134.         [ Links ]

Navár J., 2004, Water supply and demand in the lower Río Bravo/Río Grande basin: The irrigated agriculture scenario. Geofísica Internacional, 43, 3, 495-506.         [ Links ]

Rubin Y., Hubbard S.S., 2005, Hydrogeophysics. Springer, Heidelberg, 523 pp.         [ Links ]

Schleiss A., 2008, Reservoir sedimentation and sustainable development, in KHR ISI International Workshop "Erosion, Transport and Deposition of Sediments", 28 April 2008, Bern.         [ Links ]

Sharma P.V., 2002, Environmental and engineering geophysics, Cambridge University Press, 475 pp.         [ Links ]

Stout L.A., Harrington Jr. J.A., Grimshaw H.J., Shapiro G.L., 1985, Bathymetric changes in Overholser reservoir. Proceedings of the Oklahoma Academy of Sciences, 65, 69-72.         [ Links ]

Yutsis V.V., Jenchen U., de León-Gómez H., Izaguirre Valdez F., 2009, Paleogeographic development of the surroundings of Cerro Prieto water reservoir, Pablillo basin, NE Mexico, and geophysical modeling of the reservoir's subsurface. Neues Jahrbuch für Geologie und Paläontologie, 253, 1, 41-59.         [ Links ]

Vasudevan M., Sivakholundu K.M., 2007, Application of Parametric Acoustics for Shallow-Water Near-Surface Geophysical Investigations, in Abstracts of the OCEANS 2006 Asia-Pacific.         [ Links ]

Wunderlich J., 2007, Mobile parametric sub-bottom profiler systems for shallow and medium depth applications. J. of the Acoustical Society of America, 122, 5, 29-83.         [ Links ]

Wunderlich J., Müller S., 2003, High-resolution sub-bottom profiling using parametric acoustics. International Ocean Systems, 7, 4, 6–11.         [ Links ]

Wunderlich J., Wendt G., 2001, Advantages of Parametric Acoustics for the Detection of the Dredging Level in Areas with Siltation, in Proc. of the 7th Workshop on Dredging and Surveying, Scheveningen: 67–75.         [ Links ]