Although important for the eco-hydrological functioning of the floodplain, the interactions between river and floodplain are not well understood, especially for rivers in the tropical monsoon region. To explore the floodplain functioning of a tropical monsoon river system the longitudinal and transverse floodwater hydrochemical characteristics were studied in the Songkhram river (Thailand) and its floodplains. Water samples were taken during the monsoon period from 61 locations in the river and on its floodplain. Analysis of floodwater hydrochemistry revealed a significant decreasing longitudinal trend for most dissolved solids, attributable to geological differences. We also observed a significant decreasing transverse trend from river to floodplain. Nutrient concentrations revealed lower dissolved nitrogen, phosphate, and potassium concentrations on the floodplain than in the river channel, which suggests the floodplain functions as a sink for nutrients and chemical species in the river floodwater. This sink function may be related to the presence of a belt of bamboo separating the river from the floodplain, which seems to acts as a sediment trap and nutrient filter, but this needs to be verified by additional dedicated research.
River floodplains are key elements in the landscape. Their numerous and diverse natural functions and ecosystem services include providing a refuge for many species (Ward et al. 1999; Tockner and Stanford 2002; Ward et al. 2002), river water purification (Costanza et al. 1998; Keddy et al. 2009), and flood storage and control (Banerjee et al. 2013; Grygoruk et al. 2013). The hydrology and ecosystem function of floodplains are highly dynamic (Junk et al. 1989; Bayley 1995; Ward et al. 1999; Ward and Tockner 2001). The extent, depth, and duration of inundation depend on the hydrology and local topography (Steiger and Gurnell 2003; Southwell and Thoms 2011; Langhans et al. 2013), while the chemistry of floodplain water is a function of exchange processes between groundwater and surface water and the influence of precipitation (Boulton et al. 1998; Doering et al. 2013; Keizer et al. 2014). Nutrient transport in the river–floodplain system is important for the productivity and species richness of floodplain vegetation.
The interactions and exchanges between the river and the floodplain during inundation, when water, sediment, and nutrients move across the floodplain, can be described by the flood pulse concept (FPC), which was originally proposed by Junk et al. (1989) and Junk and Wantzen (2004). The rewetting of dry sediment mobilizes nutrients and (in) organic matter from locally mineralized and decomposed organic matter (Baldwin and Mitchell 2000; McClain et al. 2003). In accordance with the FPC, it is assumed that river water covers the entire floodplain during inundation, producing a homogeneous hydrochemistry over the inundated floodplain. However, it has been shown for several floodplains that the water quality is not homogeneous across the floodplain. Distinct spatial patterns in inundation water quality have been observed for temperate river floodplains in Poland (Chormanski et al. 2011; Keizer et al. 2014) and Austria (Tockner et al. 1999). Large river floodplains located from the Arctic to the Amazon also demonstrate a zone of mixing between the sediment-rich river water and the local water (groundwater and/or precipitation), defined as the “perirheic zone” (Mertes 1997). The spatial heterogeneity in the floodplains is thought to result from the presence of different water sources and the impact of antecedent moisture conditions; in turn, these may cause various processes over time, such as decomposition of organic matter, solute transport, and absorption/desorption to/from soil (Wassen and Joosten 1996; Lewis et al. 2000; Beumer et al. 2008).
The transverse transport of material across floodplains is not the only process relevant for river–floodplain ecosystems: also important is longitudinal transport. The water quality can be altered downstream along the river channel by spatial differences in geological substrate that result in varying dissolved material input to the river channel. In turn, the concentrations of dissolved material such as nutrients may be increased or decreased when river water spreads over the floodplain, affecting the floodplain ecosystems (Lewis et al. 2000). The longitudinal patterns can be explained by using the river continuum concept (RCC) (Vannote et al. 1980), which assumes that physical gradients in the river from upstream to downstream are responsible for a continuum of change in ecological processes along the river. According to the RCC, nutrient input is mainly from organic material and is expected to vary downstream along the river because sources and forms of input vary, shading and turbidity affect the penetration of solar radiation into the water column, and the biotic community adapts in response. The physico-chemical variables that most influence the longitudinal patterns in the river channel are watershed area, phosphate concentration, total dissolved solids, solar radiation, annual precipitation, the ratio of stream length to watershed area, and terrestrial litter input (Cushing et al. 1983). However, the RCC does not describe ecological processes for rivers and floodplain combined, but mainly predicts ecological processes in river channels. Also, the hydrochemistry can vary along the river due to discontinued geomorphological characteristics (Sedell et al. 1989; Tockner et al. 2003).
Recently, Humphries et al. (2014) proposed a new concept to merge the longitudinal and the transverse processes in rivers and their floodplains, called the “river wave concept”. This concept sees river flow characteristics as wave forms and characterizes them according to positions on the ascending or descending discharge limb, trough, and crest. These positions correspond to stages of water level in the river and floodplain. Longitudinal and transverse processes of the river and the floodplain ecosystems are a function of these positions, temporally and spatially.
To the best of our knowledge, unifying concepts that describe the hydrochemistry and ecological functioning of floodplains have not been tested for tropical monsoon rivers. Such rivers provide important environmental, economic, and social benefits to local communities, including biodiversity hotspots, agricultural land, and fresh water. However, existing knowledge of tropical monsoon river–floodplain systems is insufficient for their efficient conservation and management (Bayley 1995; Arthington et al. 2010). To improve understanding of the river–floodplain function in a tropical monsoon region, we examined the longitudinal and transverse spatial patterns of hydrochemistry, nutrient availability, and land cover along the Songkhram river, its tributaries and floodplain in north-eastern Thailand. The Songkhram monsoon river is characterized by a relatively natural flow, and can thus serve as a reference for tropical monsoon systems. In this research the following three questions were central: 1) What are the longitudinal (upstream–downstream) and transverse (river–floodplain) trends in hydrochemistry and nutrient availability during the flood period in the monsoon river system? 2) Do nutrient availability and water chemistry differ significantly between the main river channel and the floodplain during the flood period? 3) Are these differences related to land cover on the floodplain?
The Songkhram river, a tributary of the Mekong River, is located in north-eastern Thailand (Fig.1). It is approximately 495 km long, drains an area of 13,000 km2 and its average discharge is 226 m3 s−1 during the monsoon season and 2.3 m3 s−1 during the dry season. Precipitation records from 1980 to 2010 at Ban Tha Kok Deang, centrally located in the catchment, show that annual precipitation averages 1960 mm and ranges from 1090 to 2880 mm. The monsoon season lasts from May to September and is followed by a cool dry season from October to February that is succeeded by a hot dry season from March to April. During the monsoon season the average precipitation is 1690 mm (range 906–2420 mm); this compares with an average precipitation of 270 mm (range 80–490 mm) during the dry season (figures compiled from daily data from the Department of Water Resources, Thailand). Mean annual temperature is 26 °C and the warmest month is April (35 °C). The minimum temperature is around 15 °C from December to January.
Extensive floodplains are found in the lower part of the basin as well as along the upper part of the river. These inundate yearly due to high river discharges during the monsoon season and water backing up from the Mekong river (Blake et al. 2011). There are two major tributaries: the Nam-Yam and Nam-Uun. These join the main river in the lower basin. The river’s discharge behavior is quite natural, as there are no large dams that regulate water flow in the main channel. The average area flooded annually in the lower basin, estimated using Landsat images from the period 2000 to 2006, is 760 km2 (Thiha and Wongpakam 2012).
The land uses in the Songkhram river catchment are agriculture (65 % of the area), forest (20 %), settlement (5 %), surface water (5 %), and other (5 %) (Land development Department 2014). The floodplain vegetation community is known as “Pa Bung Pa Taam” and is dominated by a dense thorny bamboo: Bambusa flexuosa (Blake et al. 2011; Khammongkol et al. 2013).
The geology of the catchment is characterized by sedimentary rocks, dominated by sandstone, siltstone, mudstone, and claystone of the Phu Thok formation (KTpt) of Cretaceous and Tertiary age. In the upstream area of the catchment, the Maha Sarakham formation (KTms) from mid-Cretaceous is found, containing a layer of readily soluble rock salt, gypsum, anhydrite, and potash. Alluvial deposits and terrace deposits are found on the floodplain, along the river channel: see Fig.2 (Department of mineral resources 2012).
During the monsoon season from 10 to 26 September 2013 we conducted a field campaign in the Songkhram river catchment to sample floodwater from the main river channel and along transects across the inundated floodplain. Samples were taken during the falling limb of the yearly flood curve: in September 2013 the average discharge of the Songkhram river was 1220 m3 s−1, whereas in August the average discharge had been 1660 m3 s−1 (Thailand Royal Irrigation Department 2016).
We visited a total of 107 locations distributed along the entire length of the river. Accessibility was important and therefore most were at or near a bridge. Some locations in the Nam-Yam tributary were chosen because they could easily be reached by boat. The locations of the transects across the river floodplain were selected based on classification of floodwater zones from a Landsat 8 image acquired on 13 August 2013, one month before the field campaign. Five transects were visited during the field campaign, three of which were in the lower basin: one across the Songkhram river (TR-C), one across the Nam-Yam river (TR-D), and one across the Nam-Uun river (TR-H). Two transects (TR-J and TR-K) were positioned across the Songkhram river in the upper basin (Fig. 1).
To select locations for water sampling, we measured electrical conductivity (EC), total dissolved solids (TDS), temperature, dissolved oxygen, and pH in situ using a YSI 556MPS Multi-parameter Instrument (YSI Environmental 2009) that had undergone maintenance service just prior to use. Every day pH and oxygen were calibrated before being measured. Along each transect, water samples were taken in the river and at several locations across the inundated floodplain. In the floodplain zone, sampling locations were chosen in light of the EC measurements and the observed vegetation communities, so that the sampling sites captured the variation in the EC and vegetation communities.
In total, 73 water samples were taken from 61 of the 107 locations in the rivers and floodplains. Not all 107 locations were sampled because some locations were close to each other and on site EC measurement did not show notable differences. We used a Kemmerer type water sampler 10 cm in diameter and 30 cm long, with a rope attached to open the lid for underwater sample collection, and a stainless steel rod 20 cm long extending from the base of the bottle. At each sampling location 2000 ml of water was collected at ca. 30 cm below the water surface, to avoid floating debris. Samples were taken from 33 locations in the river and 28 locations on the floodplain. In addition, to obtain insight into possible stratification in the water column, a second sample was collected at ca. 20 cm from the bottom at 12 locations (4 in river; 8 on floodplain). The vegetation and land use type around each sampling location were described.
The water samples were collected in a high-density polyethylene water container and stored immediately under dark conditions in a cooler on ice. The container was pre-washed on site, with the water to be sampled, before being filled with the sample. Within the same day of collection, the samples were transported to the laboratory of the Aquaculture Research Institute, Department of Fisheries, Ministry of Agriculture and Cooperatives in Sakon Nakhon, for filtration and treatment.
In the laboratory, within 24 h of the sampling, alkalinity was measured on a 5 ml aliquot, using a chemical test kit (Merck KGaA 2013). A 250 ml unfiltered water sample had been stored in a wide-mouthed Nalgene PE bottle (250 ml) and treated with 2 ml 0.05 M sulfuric acid. These samples were analyzed for total phosphorus (TP) using persulfate oxidation digestion and spectrophotometry (Spectronic Genesys 20, Laboratory of Environmental Studies, Faculty of Environmental and Resource studies, Maha Sarakham University, Thailand).
From each water sample, 500–1000 ml (depending on filtration speed) was filtered through a 1.2 μm Whatman GF/C glass fiber filter. The filtrate was refiltered through a 0.45 μm Whatman cellulose acetate membrane filter and an aliquot comprising the first 125 ml of filtrate was then stored in a wide-mouth PE bottle (125 ml), and 1 ml of 65 % nitric acid was added. An aliquot comprising the second 125 ml of the filtrate was also stored in a wide-mouth PE bottle but was not acidified. Most samples were filtered on the day they were sampled; all samples were filtered within 48 h of collection in the field. The first and second aliquots of filtrate were kept under dark and cool conditions (approximately 4 °C) for approximately 2 days until they were transported to the GEO lab of Utrecht University, the Netherlands. The samples were in transit for 8 days. Using inductively coupled plasma optical emission spectrometry (ICP-OES), the first aliquots were analyzed for the following major cations, trace elements, and metals: aluminum (Al3+), barium Ba2+, calcium (Ca2+), iron (Fe2+/3+), potassium (K+), magnesium (Mg2+), manganese (Mn2+), sodium (Na+), silica (Si+), strontium (Sr2+), and zinc (Zn2+). The second aliquots were analyzed for chloride (Cl−), nitrate (NO3 −), nitrite (NO2 −) and sulfate (SO4 2−), using ion chromatography. Ammonium (NH4 +) and phosphate (PO4 3−) were analyzed by continuous segment flow analyzer (Seal Analytical 2000).
Statistical Characterization of Floodwater Hydrochemistry
To ascertain the variance of the hydrochemical parameters analyzed, a statistical overview was created showing the number, mean, minimum, maximum, range, standard deviation, and coefficient of variation of each parameter. To understand which combination of parameters accounted for the largest portion of the variance, we used principal component analysis (PCA) with the varimax rotation method performed on the standardized data. Next, factor scores of each sample were determined by means of regression analysis. This reduced the chemical variables to three main factors, which were determined by a parallel analysis method (Franklin et al. 1995; Peres-Neto et al. 2005). Total dissolved nitrogen (TDN) was calculated by the summation of nitrogen in NH4 +, NO2 −, and NO3 −. There were some missing values in the NO3 − dataset because concentrations were below the detection limit for some samples and some errors occurred when preparing samples. As PCA does not allow missing values, we first assumed that there was no NO2 − and NO3 − for the samples in question. Then we tested this assumption by only using NH4 + as nitrogen and using the half values of the lowest detection limits for NO3 − and NO2 −. The subsequent PCA analysis did not reveal any significant differences. We did not include total dissolved solids (TDS) in the PCA since TDS is directly proportional to the measured EC.
Determining Longitudinal and Transverse Trends
Longitudinal (upstream–downstream) trends in hydrochemistry were analyzed by plotting the scores of the three principal components against the distance to the river catchment outlet, for samples taken in the river channel. The scores of the first principal component were also plotted on a map of the catchment, to analyze their spatial distribution in the Songkhram river and its tributaries. Transverse hydrochemical trends in the river–floodplain system were analyzed by plotting the scores of the three principal components against the distance of the floodplain sampling location from the main river channel. This was done for all transects together and also for each individual transect.
Differences between river channel and floodplain concentrations of the nutrients phosphorus, potassium, and nitrogen in floodwater were analyzed by comparing box plots for all river channel samples with box plots for all floodplain samples.
Relationship between Floodplain Land Cover and Hydrochemistry
To ascertain the relationship between floodwater hydrochemistry and land cover, the land cover under the flooded areas was analyzed by first estimating flood extent and then determining the land cover for that area.
To estimate the inundated area of floodplain we used satellite images of Landsat 7 ETM+ from 17 August 2000. Interpretation of the image of the upper part of the basin was hampered by cloud cover. Therefore the floodplain area we report on in this study refers to the lower part of the catchment only. The image, which has a spatial resolution of 30 m, was visually interpreted and the flooded area was delineated using the ENVI 5.0 software package (Exelis Visual Information Solutions 2014). The date on which it was acquired, 17 August 2000, is in the third quartile of the highest precipitation records in the period 1980–2010. Thus we consider this image to be representative of average to high floods.
The land cover classification for the lower river basin was produced using a Landsat 8 OLI scene acquired on 3 January 2014 during the dry season. This image also has a spatial resolution of 30 m. It was radiometrically corrected to the top-of-atmosphere reflectance image following the USGS guidelines (USGS 2013). Land cover was determined using a supervised classification approach with the maximum likelihood classifier (Lillesand et al. 2008). This approach utilizes representative samples of particular land cover classes of interest as training regions. The training region is an area of known land cover from ground truth data assigned to the corresponding pixel(s) in the image, which the software uses as a guideline when assigning land cover classes to similar image pixels. When selecting training regions we relied on information and experience acquired on the ground during fieldwork in February 2013.
The classification accuracy was estimated by randomly taking 330 locations in the classified image and comparing them with the land cover derived by visually interpreting a high-resolution satellite image available in Google Earth acquired on 10 January 2014. To estimate the accuracy of the supervised classification, a confusion matrix was computed; the matrix compares the classification result class with the actual class of land cover as determined by visual interpretation from Google Earth.
To determine the land cover characteristics of the lower basin floodplain area we superimposed the map of inundated area on the land cover class map.
Statistical Characterization of Flood Water Hydrochemistry
Hydrochemical statistics of the sampled surface waters are summarized in Table 1. The chemistry of the water is dominated by alkalinity, Cl−, Na+, Ca2+, and Si+. On average, the coefficient of variance (CV) is 67 % over the area, indicating general great variability between the samples. The most variability was found for NH4 + and Mn2+, although concentrations were low. Low variability (CV less than 40 %) was found for temperature, pH, dissolved oxygen, and some ions (Ba2+, Fe2+/3+, Si+, Zn2+).
PCA revealed that the three main principal components explain 62 % of the overall variance in water chemistry (Table 2). The first PCA component (accounting for 44 % variance) contains most of the chemical variables, with factor scores above 0.7 for EC, Ca2+, Mg2+, HCO3 −, Na+, Cl−, K+, SO4 2−, Si+, and Sr2+. We interpret this principal component as the enrichment of water with major ions resulting from weathering and dissolution of minerals.
The second PCA component (accounting for 10 % variance) contains the variables Zn2+, TP, and PO4 3− , which correlate negatively with dissolved oxygen levels. The presence of high TP and PO4 3− concentrations when dissolved oxygen is low indicates anaerobic and/or chemical reduction conditions during which PO4 3− is released to the water. Thus, we interpret this principal component as low redox conditions enhancing dissolution of phosphorus. It is notable that this condition was observed deeper in the water column, where dissolved oxygen is lower than at the surface.
The third PCA component (accounting for 8 % variance) is associated with Al3+ and Fe2+, 3+, which we interpret as dissolution of aluminum and iron compounds from the soil.
Longitudinal and Transverse Hydrochemical Trends
Longitudinal trends in hydrochemistry were analyzed by plotting the scores of river samples on each principal component arranged from upstream to downstream (Fig. 3). Only the first component correlated significantly with the relative distance to the river outlet (r = −0.59, p < 0.05), indicating that the dissolved solids decreased in the downstream direction. The spatial distribution also shows higher scores in the upstream part of the Songkhram river and its tributaries, with lower scores in the downstream part (Fig. 4). This longitudinal trend is related to the geological substrate of the catchment (see Fig. 2). In the upstream area the river channel is cut into bedrock: the KTms formation that consists of rock salt, gypsum, anhydrite, and potash, while the main geological substrate of the floodplain is alluvium. The correlation between the smallest distances of the sample location to the KTms formation and the PC1 score was significant, with r = −0.43 (p < 0.05). This implies that the concentration of dissolved material in the water is related to the distance from their geological origin.
For the transverse trends across the floodplains using all transects (Fig. 5), a significantly decreasing trend was observed for the first component. The scores of this component correlated significantly with the distance of each sampling location to the main river channel, with r = −0.32 (p < 0.05). This means the concentration of major dissolved solids in the floodplain inundation water is inversely related to distance from the main river channel. In contrast, we found no significant longitudinal or transverse trends in principal components 2 and 3, nor did we find a correlation with the distance from the geological substrate.
The nutrient concentrations, expressed by the variables TP and PO4 3−, total dissolved nitrogen (TDN), and potassium (K+), of samples from the main river channel were compared with those from the floodplain, to better understand the spatial patterns of these ecologically important elements. The concentrations of PO4 3−, TDN, and K+ were significantly higher in the main river channel than in the floodplains (t-test, p < 0.05), but the concentrations of TP did not have significantly higher values in the river channel (see box plots in Fig. 6). This indicates that the floodplain generally functions as a sink for nutrients.
Relationship between Hydrochemistry and Floodplain Land Cover
The inundated area estimated from the Landsat 7 ETM+ image (17 August 2000) was ca. 855 km2. Its shape is influenced by the topography: in low-lying areas it extends further inland (see Figs 1 and 7) and flooded areas link up with permanent water bodies in depressions (see Fig. 8).
Ten land cover types were distinguished in the lower floodplain of the Songkhram river catchment (derived from Landsat 8 OLI data, Fig. 8). The major land cover type in the floodplain is agriculture, which is reflected in the classes rice paddy culture (both rain-fed and irrigated), plantations, and bare soil. Bare soil is usually the result of rice paddy field preparation or is land that has recently been cleared for a new plantation of rubber (Hevea brasiliensis). These agricultural land cover type are highly dynamic during the year due to anthropogenic activities. The overall map accuracy was 72 %, as validated by randomly generating locations for each map class (330 locations in total) and comparing them with ground cover assigned by eye on the basis of the high-resolution Google Earth images (see Table S1). The classification with the greatest uncertainty concerns rice paddy (45 %), which is mostly confused with the grass and herbaceous and shrub class or with the class “water”. The settlement class also shows low accuracy (50 %) as it can be confused with a similarly reflecting surface of the “bare soil” class and the “grass and herbaceous and shrubs” class. The bamboo vegetation class had high classification accuracy (90 %).
Superimposing the vegetation and land cover classes on the map of inundated areas (Fig.8) revealed that the land cover accounting for the largest proportion of flooded land was agricultural: 52 % of the flooded area was comprised of bare soil, irrigated and rain-fed rice paddies, and plantations. The class containing grass, herbaceous vegetation, and shrubs together occupied 20 % of the flooded area. The remaining categories were open water (9 %), marsh (8 %), deciduous forest (6 %), bamboo vegetation (4 %), and settlements (1 %).
It is clear from Fig. 8 that bamboo vegetation is found along the river channels and in most places consists of a belt of a few hundred meters wide, with a maximum width of 1200 m. Behind the bamboo belt, the class of grass, herbaceous, and shrubs is generally present. In the field, a narrow strip of a native thorny shrub was often observed growing next to the bamboo belt, with a gradual transition to grass and herbaceous vegetation. The irrigated rice paddy class was observed nearby water bodies that do not dry up in the dry season, such as lakes, oxbow lakes, and the main river channel. Rain-fed rice paddies were generally found further away from the river channel.
Longitudinal and Transverse Hydrochemical Trends
Our sampling strategy was designed to capture the maximum spatial variability of floodwater chemistry in the river channel and floodplain. We sampled along the main river channel as well as its tributaries. The transect locations were selected to represent variability in the floodplains in the upper and lower parts of the river basin. Water chemistry is influenced by the origin of the water and by certain natural and anthropogenic factors. The following factors are relevant: the occurrence of highly soluble or easily weathered minerals; the distance from the marine environment, which controls the exponential decrease of ocean aerosols that are input to the bordering land; the aridity (precipitation/runoff ratio), which determines the concentration of dissolved substances; terrestrial primary productivity (which controls the release of nutrients); and ambient temperature. Our hydrochemical data on the Songkhram monsoon river revealed that concentrations in the river and floodplain inundation water were low. The water was poor in dissolved solids and nutrients, and slightly acid. The dominant ion concentrations were Na+, Cl−, Ca2+, and alkalinity (HCO3 −), which are related to the weathering products of the Songkhram river catchment geology, especially the KTms formation which is the likely source of river water sodium and chloride from rock salt, calcium and sulfate from gypsum and anhydrite, and potassium from potash. The relatively soft sandstone is a source of silica.
The EC, which is a good indicator of dissolved materials in the water, was on average 73 μS/cm. This is much lower than the EC of the 3 groundwater samples we took during the fieldwork (EC average 414 μS/cm). This difference can be attributed to the river water being greatly diluted during the monsoon season by the large amounts of rainfall, which has a low EC (Meybeck and Helmer 1989). Decreased solute concentrations during the monsoon have indeed been reported in a previous study of the Songkhram river (Satrawaha et al. 2009) as well as for monsoon rivers in India (Mehto and Chakrapani 2013; Kumarasamy et al. 2014; Thomas et al. 2014).
The relatively high average coefficient of variation indicates that the hydrochemistry of the floodwater of the Songkhram monsoon river and its floodplain is very variable. The longitudinal variability of hydrochemical concentrations in the Songkran River showed a decreasing trend from upstream to downstream. We relate this trend to the upstream occurrence of the geological KTMms formation with highly soluble minerals, as substantiated by the significant correlation between PC1 score and smallest distances of the sample location from the KTms formation.
The transverse hydrochemical trend revealed solute concentrations decreasing from the Songkhram river channel to its floodplain. This was evident both from the PC1 scores, which reflected the concentrations of most elements, and from the box plots, which showed significant higher concentrations in the river channel than on the floodplain for PO4 3−, TDN, and K+. We therefore conclude our hydrochemical floodwater pattern suggests a sink function of the monsoon floodplains for dissolved solids from the Songkhram river in Thailand.
Bamboo as a Sediment and Nutrient Filter
The water column on inundated floodplains is shallower than it is in the main river channel. This allows more light to penetrate the floodplain water column, leading to higher temperatures. These conditions favor the growth of green algae and of aquatic vascular plants in the floodplain, leading to higher productivity than in the river channel. Thus the decrease in nutrients in floodwater on the floodplain might be attributed to uptake by aquatic vegetation growing in the floodwater (Lewis et al. 2000). However, this might partly be only a temporary sink, since nutrients taken up by algae will be largely released when algae die and only the portion of the nutrients taken up by bamboo and other vascular plants may be stored into a sink for a longer time.
During the classification of land cover in the flooded areas it was noted that bamboo vegetation is found in a zone immediately adjacent to the river channels. The bamboo vegetation is generally very dense, and during fieldwork, sedimentation and algae growths were observed around the bamboo stems (see Fig. 9). The clumps of bamboo along the Songkhram river reduce the velocity of floodwater, which may enable sediments in the water to settle. The bamboo is also highly productive, as evidenced by its large standing biomass. This suggests it is efficient in taking up nutrients, either directly from the floodwater or, in the dry season, from the sediment remaining after the flood. We did not find any clear data on these processes in the literature or in the field. Nonetheless, we would argue that the floodplain functions as a net sink of nutrients, mediated by highly productive bamboo. And this indicates that the river is a source of nutrients and sediment for the floodplain.
Although our results show how the river and its floodplain interact in terms of hydrochemistry, we still lack a clear pattern of transport of sediment, nutrients, and organic material. Candidate topics for future research could therefore be the pathways and transformation of particulate material in the river and floodplain, as well as the temporal variation in processes affecting transport and transformation. In addition, dedicated research should test our hypothesis that the sink function of the Songkhram monsoon floodplain is primarily related to the presence of a bamboo strip in the floodplain, which seems to act as a sediment trap and solute filter. We suggest future analyses on sediment characteristics in the river and floodplain, as this may also be important for nutrient cycling in the aquatic system and such analyses may explain the source of Fe2+, 3+ and Al3+ and the processes steering their dissolution.
Ecological and Hydrological Concepts for Monsoon River Systems
The decreasing longitudinal trend of hydrochemical concentrations in the river during flooding as observed in our study corresponds to the physical gradient from upstream to downstream as described in the river continuum concept (Vannote et al. 1980). The limited information we gathered indicates this concept may be applicable to explain the ecological functioning of our river system. The observed decreasing trend of EC from upstream to downstream may indicate a shift in the biotic community along the river, as suggested by Jiang et al. (2011). However, in order to draw conclusions about the longitudinal ecological functioning of the monsoon river system, research needs to be done on the response of the biotic community to the hydrochemistry gradient.
The river/floodplain system we studied is also subject to transverse processes affecting the chemistry of the floodwater on the floodplain. The flood pulse concept (Junk et al. 1989), explains the ecological functioning of large river floodplain systems in terms of lateral exchange of water, sediment and nutrients between the river and the floodplain. In our study, the river functions as a transportation route and source of dissolved material for the floodplain, including nutrients PO4 3−, TDN, and K+ as postulated by the flood pulse concept. It is therefore likely that both concepts are applicable to explain the ecological functioning of our river system during the flood period. This is in line with the suggestion of Humphries et al. (2014), who propose the river wave concept that merges the RCC and FPC and combines it with the riverine productivity model (RPM) proposed by Thorp and Delong 1994. The RPM postulates that the river bank vegetation is highly productive due to nutrient input from the river, which may be applicable to the bamboo zone we described.
Although some general observations can be made based on our data for one monsoon river, there is a need for further data collection in monsoonal river systems to verify to what extent different river concepts also hold for river systems of this type.
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Many people contributed to this study during the preparation stage, fieldwork, laboratory analysis, and data processing. We thank Pinploi Sirivarikul for her fieldwork assistance in Thailand. Rojchai Satrawaha, Rachanee Nam-martra, and Panida Laotongsan from Walai Rukhavej Botanical Research institute, Mahasarakham University, Thailand are acknowledged for the fieldwork and laboratory facilities and Sathaporn Kavinate from the Department of Mineral Resources, Thailand for reviewing the geological map. We also wish to thank the Inland Aquaculture Research Institute, Department of Fisheries, Ministry of Agriculture and Cooperatives, Sakon Nakhon, Thailand for providing laboratory facilities and accommodation during the fieldwork. This research was partly supported by a grant from the Thai Government Science and Technology Scholarship Students program. Joy Burrough was the professional language editor of a near-final draft of the paper.
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Walalite, T., Dekker, S.C., Keizer, F.M. et al. Flood Water Hydrochemistry Patterns Suggest Floodplain Sink Function for Dissolved Solids from the Songkhram Monsoon River (Thailand). Wetlands 36, 995–1008 (2016). https://doi.org/10.1007/s13157-016-0814-z
- Ecological function
- Spatial pattern
- South-East Asia
- Flood pulse concept
- River continuum concept