Notice: Wiley Online Library will be unavailable on Saturday 30th July 2016 from 08:00-11:00 BST / 03:00-06:00 EST / 15:00-18:00 SGT for essential maintenance. Apologies for the inconvenience.
 A fundamental, and often intriguing question, in hydrology is “where does the water go?” This becomes particularly difficult to observe when water arrives at the ground surface and infiltrates into soils. The development of rapid, campaign-style imaging methods that do not need to be left in situ are therefore of great interest in tracking subsurface hydrological redistribution. We present a novel geophysical imaging approach identifying spatiotemporal variation consistent with soil water redistribution in a tropical deltaic soil. The intention is to provide additional insight into spatiotemporal soil hydrological/biogeochemical processes. The bulk soil electrical conductivity response (ECa) is primarily controlled by the clay content and type, the ions retained in the soil solution (ECe), and the soil water content (θ). Clay content can be assumed to be temporally static, whereas θ and ECe are temporally dynamic. By imaging over time, we can attempt to tease apart these contributing factors. In nonsaline soils θ is the major contributor to temporal changes in ECa. By exploiting an intensive rainfall event (75 mm), with time series spatial ECa measurements, before and after the event, we were able to identify zones of water depletion and accumulation and to provide an indication of the time required for the soil to return to its prior state. In addition, locations with more clay and salts were identified through response surface-directed soil sampling. We found important spatiotemporal variation across the level 4 ha field site that from visual inspection appeared uniform.
If you can't find a tool you're looking for, please click the link at the top of the page to "Go to old article view". Alternatively, view our Knowledge Base articles for additional help. Your feedback is important to us, so please let us know if you have comments or ideas for improvement.
 Where does the water go? This is a fundamental question within hydrology, particularly in the context of the infiltration and redistribution of water in soils following precipitation. Once water enters the soil there is a severe limitation in our ability to track and visualize where, and how, water moves. This is particularly difficult in developing countries where sensors and monitoring equipment can rarely be left in place. Therefore, the development of rapid, campaign style, imaging methods that do not need to be left in situ are of great interest to track subsurface hydrological processes.
 Hydrologists have been inventive in developing models and methods of predicting the movement of water in the subsurface. Fortunately, water moves according to potential gradients, mainly gravitational and matrix forces. This has allowed the development of theories and models to describe infiltration [Philip, 1969] and soil water dynamics [Daly and Porporato, 2005]. The development of advanced sensor technologies for determining soil moisture [Robinson et al., 2008a; Huisman et al., 2003] and soil water potential at a point has allowed the testing of 1-D infiltration theory in both the laboratory and field [Si and Kachanoski, 2000; Noborio et al., 1996]. However, even with these advances, there remain significant gaps in our understanding and ability to measure infiltration and redistribution processes at the field scale. This is especially true in developing countries where monitoring equipment is vulnerable. Even with the collection of point data, the problem is often encountered, that the scale of the point data is incommensurate with hydrological process models [Beven, 2001]. This results in a lack of good quality hydrological process data, especially for the intermediate scales [Western et al., 2002].
 The flow of water through a 3-D landscape presents a much greater challenge. As topography becomes steeper so gravity dominates the movement of water. Digital elevation models (DEMs) have been used to determine flow paths and can be combined with hydrological models to estimate the saturation index across the landscape [Lane et al., 2004], but essentially remains a black box. A major limitation to advancing our understanding of subsurface flow processes is the lack of spatial data to test models, many of which have increased in complexity, but offer a range of nonunique results [Beven, 2001]. One measurement method that has proved particularly valuable, and continues to develop, is the use of tracers. This ranges from the use of dyes [Flury and Wai, 2003] to the measurement of isotopes [Clark and Fritz, 1997]. However, dyes are limited in subsurface applications to small areas and require destructive sampling. Other tracers, including chemical tracers such as chloride and bromide, and isotopic tracers can confirm the arrival time of water and with sampling via wells or destructively can be used to obtain a snapshot of the spatial pattern of a hydrological process [Flury and Wai, 2003, and references therein]. However, none of these methods provide an image of hydrological processes at the field scale, all of these techniques are either destructive or expensive, requiring extensive well sampling and chemical analysis to try and build up a spatial picture.
 Some may question the need for spatial imaging; however, in interdisciplinary studies where hydrology is a key control on biogeochemical processes, images, from which hydrological processes can be inferred, or the spatial extent of processes delineated, are invaluable in planning and interpreting field-scale research. Our rationale for developing a more advanced soil hydrological imaging method is to fill this need, particularly for biogeochemical studies, to identify and delimit spatial zones of soil moisture accumulation and depletion, and identify areas with the most obvious “changes” occurring. This methodology could be applied to the study of many soil processes including, pesticide movement or contaminant flow; however, our particular interest in Cambodia is to understand processes that govern the release of arsenic [As] in soils to groundwater.
 In southeast Asia contamination of groundwater by [As] has become a major humanitarian disaster with millions of contaminated drinking water wells [Ahmed et al., 2006]. A range of processes have been postulated for the release (desorption) of [As] from the solids into the pore water; the onset of reducing conditions and ensuing reductive dissolution of [As]-bearing Fe (hydr)oxides is generally ascribed as the dominant mechanism [Ahmed et al., 2004; deLemos et al., 2006; McArthur et al., 2001]. Organic carbon, transported from the surface [Harvey et al., 2002], and more recently, soil and near-surface sediment redox processes have been identified as contributing mechanisms of [As] release to groundwater [Polizzotto et al., 2008, 2005]. The purpose of this paper is not to enter into this debate about the source of [As], but to assist the biogeochemist in identifying potential zones of hydrological/biogeochemical change in soils, particularly soil moisture accumulation and depletion across a 4 ha deltaic field site. It must be remembered that in developing countries it is particularly difficult to obtain monitoring data because of difficulty with securing equipment. The development of rapid, campaign-style imaging methods that do not need to be left in situ in the field is of great interest for this style of research.
 The aim of the work was to observe hydrological processes by obtaining spatial images in time series that could be used to interpret hydrological processes across the field site, so as to understand spatial patterns in behavior. In particular to provide qualitative answers to the following questions, which are often of interest at many field sites.
 1. In which area of the field site is drainage and change in conditions most apparent?
 2. Following a precipitation event which locations are wettest and then return to prerainfall conditions most quickly, and how long does this take?
 3. Where are the locations where clay is most likely to have accumulated?
 4. Are there locations where soluble salts build up?
 The answers to these questions may help inform researchers as to how representative chosen sampling locations are, or may be used to guide soil sampling. From the biogeochemical view point, knowing where water depletes or accumulates gives some indication of likely redox conditions. Knowing the locations with more clay is important as greater biogeochemical reactive surface area becomes available; and identifying locations with more soluble salts is useful as adsorbed species may be released because of mass action. At this stage in the research the intention is to provide qualitative answers. As the research progresses the plan is to try to link hydrological and geophysical models to interpret the data more fully.
 Our research, over the duration of a month, was used to obtain a series of images using multiple EMI surveys following a rainfall event. Inference of hydrological processes was based on changes in the soil electrical properties. The collection of multiple surveys in a time series allows for rank stability analysis of the data [Vachaud et al., 1985], allowing us to locate areas where the bulk soil electrical conductivity (ECa) is consistently higher or lower through time and observe change. Concurrently we performed a calibration with an EMI drainage experiment to determine the ECa dependence on θ.
2. Theory of Electrical Measurements in Soils
2.1. Soil Electrical Properties
 The measurement of ECa depends mostly on a combination of three distinct soil properties, θ, soil texture (clay %), and the soil solution extract electrical conductivity (ECe) [Friedman, 2005]. The dependence of ECa on ECe has meant that EMI is the primary field technique used for identifying soil salinity [Corwin and Lesch, 2003]. EMI mapping protocols have been developed in this regard to provide quantitative estimates of soil salinity [Corwin and Lesch, 2005]. The dependence of ECa on soil texture, θ and ECe means that it can be difficult to determine, with certainty, which property is dominating the signal. Calibration methods using response surface and directed soil sampling have been developed for saline soils by Lesch et al. [1995a, 1995b] to interpret patterns using correlation and soil samples. In this work, in addition to using directed sampling, we also use a different approach, we assume that clay % is unchanging across the field site, i.e., it is temporally static, whereas θ and ECe will be temporally dynamic. Because these soils are considered nonsaline, we assume that changes in θ will govern the ECa response [Mualem and Friedman, 1991]. In addition it is important to note that increasing θ, ECe and clay % all act to increase the ECa response. This is advantageous in the study of [As] as all these factors may work together to enhanced [As] risk.
2.2. EMI Measurement Method
 Electromagnetic induction (EMI) is particularly suited to field-scale soil imaging work. The method is rapid, noninvasive and can be automated to collect georeferenced data. Unlike remote sensing methods, penetration depths into the soil vary from integrated averages of a few tens of centimeters to several meters depending on the transmitter and receiver spacing and orientation [McNeill, 1980; Callegary et al., 2007]. EMI is becoming more widely used in soils research [Robinson et al., 2008b]; however, it has not been widely adopted in process hydrology, or combined with biogeochemical studies, other than soil salinity research.
3. Materials and Methods
3.1. Site Description
 The study site was located in Kandal province southeast of Phnom Penh, Cambodia. It was situated between the Mekong and Bassac rivers (105.03963 latitude, 11.4996583 longitude) at an elevation of ∼5 m above mean sea level (Figure 1). The region is characterized climatically by a wet and dry season. Following the snowmelt from the Himalaya, water levels rise in the rivers and the fields become flooded. With the onset of the dry season water levels decline, the fields emerge, and are used for agricultural production in the form of rice and vegetables. The area is full of small fields which are irrigated by hand using watering cans. Initially it was feared that this may influence EMI readings, but the irrigation is frequent and shallow, water penetrating no more than 5–10 cm, whereas the EMI in the vertical orientation responds to depths of 40–100 cm. The seasonal flooding flushes any salts from the soils that may build up from the previous growing season. This area is the remnant of an oxbow system, now abandoned with the new river course. The use of the NLT Landsat 7 pseudocolor image (Figure 1) indicates the structure of the abandoned oxbows, shown in the yellow circles. Many of these remain saturated throughout the dry season and provide a supply of water for irrigation.
 The Mekong delta floodplain is roughly 62,500 km2 [Nguyen et al., 2000] and the upper 7 to 20 m of sediment has been deposited as a prograding deltaic sequence in the past 6 ka [Ta et al., 2002] following the most recent sea level highstand. Below surficial overbank clays, Holocene sediments representing delta progradation include organic-rich silts, sands, and clays; the gray sand sediments encompass the majority of wells within our field area and are those with which high dissolved [As] concentrations are typically associated [Kocar et al., 2008]. Quaternary sediments underlay the Holocene sediments and were deposited during delta aggradation [Ta et al., 2002]. The region of our site is characterized by elevated levees along river banks receding to a native wetland basin between the two rivers. The primary water-producing fine gray sand aquifer at our field site typically extends to >50 m depth and is overlain by a 3 to 20 m thick red and gray clay unit. We have installed a network of 80 wells and 10 surface water monitoring sites that are distributed throughout the basin area between the two rivers; [As] exists at concentrations above 100 μg/L nearly universally in the region across the flood plane except where local mixing with river water or flushing occurs [Kocar et al., 2008]. The abandoned oxbow channel, which is the focus area for this study, has underlying [As] concentrations generally above 500 μg/L and hydrologic analysis reveals this area as a prime contributor to aquifer recharge [Polizzotto et al., 2008; Benner et al., 2008].
3.2. EMI Mapping and Calibration
 EMI soil imaging surveys were carried out between 15 March and 3 April 2007. A DUALEM-1S EMI sensor with a 1.1 m coil spacing was used during the work [Abdu et al., 2007]. The sensor was carried at a height of about 25 cm above the soil surface. Using data collected from the EMI coils in the vertical orientation the instrument integrated most of its measurement over the top meter of soil [Abdu et al., 2007], with the greatest sensitivity in the top half meter. The instrument was connected to a Trimble ProXT (Trimble Inc, San Jose, California) global positioning system (GPS) via a portable Allegro field computer (Juniper Systems Inc, Logan, Utah). Computer software allowed the simultaneous collection of the GPS location and the EMI signal. Measurements were made at 2 s intervals while traversing the field site at approximately 4 m intervals. The detailed map of the field site, situated between two inundated abandoned oxbows, is shown in Figure 2. A line of small ∼2 × 2 m ponds run along the center of the field; these are used to store irrigation water pumped from the abandoned oxbow lakes. One of the EMI route maps is shown on the right indicating the density of measurement over the site; approximately 1100 measurements were made for each image.
 The first EMI image was made on 15 March 2007 toward the end of the dry season. On the evening of 19–20 March a 75 mm rainfall event occurred. The next image was made on 20 March immediately following the rainfall event. Subsequent images were obtained on 21, 22, 23, 24, 26, and 30 March and 3 April. Soil temperatures were measured before and after measuring and did not change from 30°C, consistent with the tropical climate. Therefore, no temperature correction was needed for the data.
 Concurrently a calibration experiment was run to determine the EMI response to drainage of soil moisture. A 2 × 2 m bunded experimental plot was constructed at the location marked by the infiltration experiment in Figure 8. A ThetaProbe (DeltaT Devices, Burwell, Cambridge, United Kingdom) was buried in the soil at 40 cm. Bulk density measurements were made using soil cores and oven drying to determine the soil porosity (ϕ = 0.41). The EMI instrument was placed in the middle of the plot at a height similar to the mapping height by placing it on 2 bricks. Measurements of ECa and θ were made when the soil was dry, before the rainfall event. After the rainfall event the experimental plot was flooded with water which was allowed to infiltrate into the soil over a 2 day period to ensure saturation. During the rainfall event the soil received 7.5 cm of water, we subsequently applied a further 50 cm of water to ensure saturation. Within 24 h the soil had reached a water content of 0.401 m3 m−3, this water content was maintained during the addition of water over the following 24 h and considered to reflect the steady state water content. The value was also in close agreement to the porosity (0.41) determined from the bulk density samples. After 48 h the soil was allowed to drain naturally and ECa and measurements of θ were made over the following 3 weeks.
3.3. Soil Sampling and Arsenic Measurements
 Soil samples were obtained as part of a larger sampling effort at nine locations across the field site. The sampling locations were identified using the EMI response surface and the directed soil sampling approach described by Lesch et al. [1995a, 1995b]. Soil samples were taken from 0 to 30 cm and from 30 to 60 cm depth. The samples were subsequently analyzed for θ by oven drying at 105°C. Subsamples were analyzed for soil texture using the sedimentation method for the particle size analysis [Gee and Bauder, 1986]. ECe was determined by making a saturated paste and extracting the solution and measuring its electrical conductivity [Rhoades, 1982].
3.4. Statistical Analysis
3.4.1. Data QA/QC
 The preliminary data analysis included a data quality check and a data cleaning procedure. As the field computer records data every few seconds it is important to go through the data and remove any points where the instrument was stationary, for instance at the beginning or end. This is done quite simply by viewing the data as a time series and checking the data against the GPS speed and removing values of 0 m s−1 and the low values surrounding them. The second check examines the magnitude of the ECa response, any negative values are removed and the surrounding data points checked for consistency with previous data points. Metal watering cans used for irrigation can cause negative and positive anomalies in the EMI response. These were easily removed by plotting the data as a time series and picking out the characteristic blips.
3.4.2. Mapping Data Using a Block Kriging Procedure
 Once the data were processed, analysis of data mean, variance, and distribution were conducted. The assumption with kriging is that of a multi-Gaussian or normally distributed input data set. This can be achieved by transforming the data using a normal score transform to obtain a normal distribution with a mean of 0 and a variance of 1 [Goovaerts, 1997]. We performed this using the analysis package SGEMS [Remy, 2005]. Variograms were fitted to the data and then block kriged on a 2 × 2 m grid using Vesper [Walter et al., 2001], which allows the use of a nonuniform field boundary, and kriging using the local variogram. Finally the data were normal score back transformed using SGEMS to produce the final kriged ECa maps.
3.4.3. Temporal or Rank Stability
 Statistical analysis of nine kriged ECa maps were conducted using differencing and the temporal or rank stability procedure described by Vachaud et al. . In this procedure the difference Δij of each individual observation Sij to the average for the respective sampling time j is calculated with
And the relative difference is calculated by
For each sampling location an average relative difference is calculated by
for the nine sampling campaigns as well as its standard deviation σ. In the present study, the relative differences are shown in a georeferenced manner [e.g., Wendroth et al., 1999]. In this way, the relative magnitude of the variable and its variation is known with respect to the location within the field and with respect to the behavior of neighboring locations.
4. Results and Discussion
4.1. EMI Dependence on θ
 The dependence of ECa on θ, measured using the EMI sensor, was demonstrated using a drainage experiment; the results are presented in Figure 3. The clay % at this location was 34% and the ECe was 0.6 dS/m, typical of the irrigation water applied to the site from the abandoned oxbow lake. The results, measured over a period of 3 weeks, with a consistent soil temperature of 31°C show an almost linear dependence of ECa on water content over this range of θ. The result is not a unique calibration for the whole field site, and thus water content cannot be determined, with certainty, from the ECa map. The slope of the graph may alter with increasing ECe, as will the intercept of the trend line, moving up or down depending on the clay % or ECe. The use of a linear trend line indicates a negative intercept, this occurs because the calibration would become increasingly nonlinear as the soil dried further [Mualem and Friedman, 1991]. Clearly, the data presented indicates a strong dependence of ECa on θ during drainage.
4.2. Spatial Correlation
 The normal score semivariograms (Figure 4) demonstrate strong spatial correlation (data for all 9 semivariograms are presented). Double spherical semivariograms were fitted to the data in order to capture the strong correlation at less than 20 m. The nugget and range of the variograms (Table 1) indicate that the nugget is higher, and the range shorter, when the soil is dry. For the driest soil on 15 March the range is about 10 m, increasing to about 20 m when the soil is at its wettest. This is similar to the pattern observed for θ measurements made in small watersheds, where the pattern becomes more random (disconnected) when the soil is dry [Western et al., 1999].
Table 1. Variogram Range for the Double Spherical Fitted Variograma
Range is in meters.
 Four of the resulting kriged maps are presented in Figure 5. The locations with higher ECa values are shown in dark red (>70 mS/m), the lowest ECa values are shown in dark blue (<20 mS/m). On 15 March (M-15) the northern end of the field had the lowest ECa values and the southwestern side had the highest. The 21 March (M-21) map follows a day after the 75 mm rainfall on the evening of 19–20 March (M-19/M20). Most of the blue zone (<30 mS/m) disappears, and the area in red (>70 mS/m) dramatically increases. This pattern persists through the end of March, and slowly the dark blue areas in the northern end of the field begin to reappear by 3 April (A-3).
 ECa values for the different days can be compared after the completion of kriging. ECa is strongly dependent on θ, demonstrated in Figure 3 and through the changes in Figure 6. The histograms (Figure 6) indicate that the ECa does not reach a maximum until M-21, a couple of days after rainfall. The red and black lines indicate the general extremities of the observed data and demonstrate that the shape of the histograms change from being positively skewed when the soil is dry (red) to negatively skewed when the soil is wet (black). Noticeably, the soil does not reach its highest values of ECa immediately following wetting. The maximum values are reached 4–5 days following the wetting. This suggests that it takes more time for the water to penetrate into the fine textured soil which continues to increase in ECa over the 5 days following the rainfall. By A-3 (blue), 16 days later, the soil reached an intermediate stage between wet and dry.
 This interpretation is supported by the spearman rank correlation coefficients for the kriged data (Table 2). They show a lag in the ECa response with the highest correlation occurring on M-21. The fact that the correlations are high before and immediately after rainfall, indicates a step increase in ECa with the increase in water content. However, following the peak ECa on M-21 the correlation begins to decline, as the time increases from the initial event and water redistributes in the subsurface. By the end of March/early April the correlation with M-15 begins to increase, as the soil dries, returning to similar conditions prior to wetting.
Table 2. Spearman Rank Correlation Coefficient for the Maps of Kriged Data for the Different Mapping Days
4.3. Difference Mapping and Temporal Stability
 The data collection on multiple days allows the data to be presented as a series of differenced time-lapse images. In Figure 7 the eight maps following the rainfall are compared to the map for dry soil (M-15) by subtracting it from the respective day. In this way we identify zones where the ECa is higher (in red) and zones where the ECa is the same or lower (in blue). Clearly, we can see the emergence of a zone with higher ECa along the southeast edge of the field, which grows in size up to M-24 and dissipates thereafter. By A-3 three quarters of the field has returned to values similar to those found on M-15. However, the southeast portion of the field remains consistently higher than before. The dark blue areas that occur at the edges of the field (0 to −10 mS/m) in the difference map indicate locations where the ECa decreased. This most likely occurred because of some leaching of ions in the days immediately after rainfall. Most of these locations at the edges of the field are close to water, either in the drainage channels or ponds, and thus evapoconcentration can occur at these edges resulting in soluble salt build up, which is quickly washed away by the rainfall.
 The temporal stability analysis of the nine maps provides us with an alternative way of looking at the data (Figure 8). Hand dug irrigation ponds (marked by circles on Figure 8), about 2 × 2 m and 1 m deep, are filled every few days with water from the abandoned oxbow lakes. The red dots indicate soil sampling locations and the three numbers associated with each sampling point indicate clay %, θ, and ECe.
 The temporal stability varies by as much as 25 mS m−1 on either side of the field average ECa. The red areas indicate locations that are consistently higher than the field average. The areas in blue show the locations that are consistently lower than the field average. We interpret this map to indicate a general transition in soil texture across the field with a combined increase in ECe and clay % at the southern end of the field which acts almost as a sump. Clay percentages in the blue area tend to be in the low 30s, in the red areas these values increase into the 40s. The change in water content across the field is also consistent with this perceived textural variation, being lower in the blue areas and higher in the red areas.
 The standard deviation of the temporal stability map presented in Figure 8b shows strong patterns. The locations of greatest change are associated with particular features of the field, such as the irrigation ponds in the center of the field, which also represent the perceived watershed in the field. Notice that the red patch near the black triangle, indicating the location of a ponded infiltration experiment, migrates to the NE (black arrow). This indicates that with the addition of so much water a lot of it went laterally. In contrast the two irrigation ponds toward the southern end of the field migrate to the NE and SW, either side of the perceived watershed. Red patches also occur at the locations where the irrigation water is pumped from the oxbow, where the pumps leak water leaching the soil, and at the edges of the drainage channel at the northern end of the field.
4.4. Soil and Surface Water Sample Data
 In addition to the geophysical imaging, soil samples from the locations indicated on the map in Figure 8a were analyzed for clay %, ECe and θ (Table 3). Given a snapshot sample, and varying texture and ECe across a field, clay % and ECe were expected to give the higher correlation with the ECa signal. Although ECa is strongly dependent on θ (Figure 3), the sampling on a single day, at a point in time, does not capture the temporal change in θ given different texture-dependent calibrations. Multiple linear regression indicated ECe as more significant than clay %. Simple linear regression of each individual variable gave an r2 of 0.68 for ECe, 0.44 for clay % and 0.24 for θ. This indicates that ECe and clay % dominate the signal response. Surface water measurements from the oxbows and from flood irrigated plots at the south of the field also indicated a strong increase in surface water EC toward the southern end of the field (Figure 9b). This is consistent with this location acting as a drainage sump. The highest surface water value of 242 mS/m (2.42 dS/m) was found in one of the flood irrigated plots and was considered to be high because of evapoconcentration. Water in the oxbow to the NE generally had EC values ∼40 mS/m, 6 times lower. The areas with increased surface water EC were also consistent with higher pH values. pH values increased to ∼8, close to the equilibrium value with calcium carbonate (Figure 9c), calcium being the dominant cation in the surface waters.
Table 3. Data Corresponding to the Sampling Sites Shown in Figure 7a
Data are shown from top to bottom and from left to right. Electromagnetic induction (EMI) values are given in mS/m, and VWC is given in m3 m−3. EMIv is vertical induction, and EMIh is horizontal induction.
4.5. Geochemical Interpretation of EMI Maps and Preliminary Arsenic Sample Data
 A range of questions were posed in the introduction with regard to assisting the biogeochemist to interpret the soil processes at the field scale. In any biogeochemical study where point samples are made, the question remains as to whether the sampling locations are representative of that general location. The novel approach presented in this work has been to measure the spatiotemporal response of soil ECa as a surrogate for monitoring soil hydrological processes during drainage. The first question, “in which area of the field site is change in conditions most apparent?,” can be answered by Figure 8b, where we identify locations with large standard deviations, indicating that the ECa response is most variable in these locations. The greatest variability is associated with the irrigation ponds, consistently drained and refilled with water, and the edges of the field site where water moves into field drains. The second question, “in which part of the field site does water drain more rapidly, and following a precipitation event which locations return to prerainfall conditions most quickly, and how long does this take?,” can be inferred from Figure 7. This is based on the assumption that as the θ increases so the difference between wet and dry ECa increases. As the soil drains the ECa is expected to return to a value close to the antecedent ECa when the soil was dry. It can be seen that the coarse textured soils in the northern end of the field return to their previous values most rapidly, turning from yellow to pale blue, the mid section of the field has returned to its previous state by April, but the southern end of the field remains well above its initial state by April, though showing a general decline. The answer to the question, “where is the soil most likely to be wettest the longest?,” is toward the southern end of the field. Observation confirmed this as the northern end of the field was unsaturated in the top 30 cm of soil by April but soil at the southern end remained saturated. Answering the question “where are the locations where clay is most likely to have accumulated?” is never easy. The traditional soil survey approach would be to use features in the landscape, color and texture samples to try and delineate this. The EMI map provides an extra layer of information in a landscape largely devoid of topographic difference or clear soil boundaries. Combining the EMI map and the texture sample locations indicates a general increase in the clay % trending from the northern end of the field site to the south. This makes some sense in that the southern end is covered by water for the longest period, as evidenced by the north–south crop transition from vegetables and herbs at the northern end of the field to rice at the southern end. This means that at the northern end there is less time for the fine clays to settle from the flood waters, there being more time for this to occur at the southern end. The build up of soluble salts also appears to follow this general north–south trend with the higher levels toward the southern end of the fields. The longer periods of soil saturation facilitate greater evapoconcentration. We tested the surface water as it transitions from the abandoned oxbow lakes to the flood irrigated fields. Figure 9b shows that the surface water in the flood irrigated fields at the southern end of the field site had EC values two to three times greater than the water in the oxbow lakes. The data provided by the combination of the EMI time-lapse imaging, and the soil samples provided the geochemical researchers with a unique spatiotemporal perspective on the hydrological and soil processes occurring on the field site.
 The information provided by the EMI imaging provided a geospatial data set to assist in locating contrasting sites for sampling [As]. EMI drastically improves the spatial (and temporal) coverage of an area when combined with other methods. The major contribution of the EMI method is to provide, with more confidence, areas of interest for direct sampling rather than replace the sampling methods (i.e., we cannot infer [As] concentrations, but on the basis of the EMI data we can propose areas that might be of interest). Total [As] concentration data from 2 nested well locations [Kocar et al., 2008] are indicated in Figure 8a by the black squares marked by X and Y. X is toward the low-ECa region of the field and Y is in the high-ECa region of the field. The results from the EMI survey assisted in locating the second nested well location (X, Figure 8a) to contrast with the existing nested well location at Y. X was located as far into the northern end of the field site as the constraints (landowners permission) would allow. The hypothesis being tested by the biogeochemistry research team was that changes in soil redox conditions, due to annual wetting and drying cycles, leads to the desorption of [As] from the solids into the pore water. The onset of reducing conditions and ensuing reductive dissolution of As-bearing Fe (hydr)oxides leads to the mobilization of [As] from soil particles into the soil solution [Polizzotto et al., 2008; Polizzotto et al., 2005]. As a result the biochemists were trying to identify locations where clay %, ECe and θ were higher for longer periods. The implication being that these locations would act as a better source for [As] that might steadily migrate further down into the sediment, thus leading to higher observable concentrations under these locations. Recent work suggests that this is a reasonable assumption, with higher EMI signal responses having shown correlation to locations with [As] in groundwater during research in Bangladesh [Aziz et al., 2008]. Our research makes no attempt to answer the question of whether this hypothesis is true, but simply assisted in identifying areas that contrasted in their hydrological behavior (wet and dry).
 Preliminary [As] concentration values from the two nested well locations did differ noticeably with increasing depth (Figure 10). The values at the southern Y location was consistently higher than at the northern location, X. The EMI images proved valuable and are encouraging, indicating that valuable insight can be obtained for interdisciplinary studies. Further research should be conducted over a wider area to determine if any observable relationship exists between the geophysical signal (ECa) and [As] concentration found in sediments in this area. Regardless of the processes governing the release of [As] into aquifers, establishing an empirical link between a geophysical signal and [As] concentrations in sediment pore waters could prove immensely helpful in improving the sighting of drinking water wells from the humanitarian perspective.
 We demonstrate that EMI can provide a rapid, campaign-style imaging method that does not need to be left in situ but still provides invaluable insight into subsurface hydrological processes. We present a sequence of EMI time series geophysical images of a 4 ha deltaic field site. The spatiotemporal images are used to interpret soil hydrological processes in a tropical deltaic landscape, devoid of topographic features that could assist in interpreting soil hydrological behavior. The imaging was conducted before and after a rainfall event and the subsequent natural drainage and redistribution. Data is interpreted using differencing in time and using rank stability analysis to identify contrasting locations where the most substantial change occurs in the geophysical response. The imaging provides qualitative visual insight into the hydrological redistribution processes occurring within the soils of the field site. The novel methodology is particularly suited to campaign style field work in developing countries, where time and data acquisition security are major issues. We identify zones which exhibit the most “change,” these are interpreted as locations consistent with soil moisture depletion, or locations from where water appears to drain and leach salts. The southern end of our 4 ha field site shows behavior consistent with a drainage sump, and liable to enhanced solution EC due to evapoconcentration. This interpretation is consistent with EC values measured from surface water and with the cropping patterns in the location. The EMI data was used to assist in locating a second nested well site so that it showed the most contrast between the soil ECa data. [As] concentrations from the well data from the two locations showed increasing divergence with depth, the controlling processes are not explained, but the new imaging approach shows good potential for assisting biogeochemical researchers in assessing the spatiotemporal characteristics of a field site from which they collect point samples.
 We are grateful to A. Falen at the University of Idaho Pedology Lab for textural analysis. We would like to also acknowledge all those who assisted in this work in Cambodia as Cambodia Resource Development International (RDIC).