A comparative view of inundation patterns in the large floodplains of South America was derived by analysis of the 37-GHz polarization difference observed by the Scanning Multichannel Microwave Radiometer (SMMR; Nimbus-7 satellite, 1979–1987). The following floodplains were analyzed: (1) mainstem Amazon River floodplain in Brazil; (2) Llanos de Moxos (Beni and Mamoré rivers) in Bolivia; (3) Bananal Island (Araguaía River) in Brazil; (4) Llanos del Orinoco (Apure and Meta rivers) in Venezuela and Colombia; (5) Roraima savannas (Branco and Rupununi rivers) in Brazil and Guyana; and (6) Pantanal wetland (Paraguay River) in Brazil. The maximum areas subject to inundation in each region, which include permanent open waters of river channels and lakes, were as follows (in km2): mainstem Amazon 97,360, Moxos 92,094, Bananal 58,550, Orinoco 107,530, Roraima 16,530, and Pantanal 130,920. The duration of inundation was correlated with the maximum area inundated. Predictive relationships between flooded area and water levels in the nearby rivers allowed extension of the inundation record over nearly a century for the Amazon and Pantanal and several decades for the other floodplains. Interannual variability in the maximum extent of inundation is greatest in the Pantanal, followed by Roraima and Bananal. Based on these extended records, the long-term mean inundation areas (in km2 and including rivers and lakes) were as follows: mainstem Amazon 46,920, Moxos 29,460, Bananal 13,110, Orinoco 34,700, Roraima 3,480, and Pantanal 34,880. This information is fundamental for hydrological, biogeochemical, and ecological studies of these floodplain-river systems and will improve estimates of methane and other trace gas emissions to the atmosphere from these vast wetlands.
 Extensive floodplains are associated with the large rivers in South America, and in contrast to the more populated regions of the world, most of these floodplains retain their natural hydrological characteristics. Inundation of floodplains along the larger rivers tends to occur as a single annual flood pulse that lasts for months [Junk et al., 1989]. Where floodplains are a significant component of the fluvial system, they can alter the transport of water and dissolved and particulate materials from upland watersheds through river systems to the sea. Water from riverine overflow or local precipitation and runoff that passes through floodplains is delayed in its transit through the fluvial system, increasing losses by evapotranspiration. During residence in floodplains, floodwaters frequently undergo substantial biogeochemical modifications under the influence of processes such as sedimentation, nutrient uptake by the biota, and changes in redox conditions [Lewis and Saunders, 1989; Richey et al., 1989; Mertes et al., 1996; Hamilton et al., 1997].
 The maximum extent of floodplain inundation, even if attained only occasionally, delineates the floodplain ecosystem because occasional floods shape the geomorphology [Mertes et al., 1996], exert control over the plant and animal life [Junk et al., 1989], and impact human occupation and land use [Junk et al., 2000]. The productivity of fisheries in tropical rivers is correlated with the extent of seasonal floodplain inundation [Welcomme, 1985]. Ecologists are interested in the seasonal timing, predictability, and interannual variability in the flood pulse because those features affect the ability of the biota to cope with and benefit from the inundation, and thereby influence which plants and animals can inhabit a particular floodplain.
 The degree of seasonal desiccation of a floodplain during the dry season determines the amount of refuge that persists for aquatic life as well as the expansion of terrestrial habitat, although in some cases the desiccation is sufficiently severe that soil moisture or periodic burning becomes limiting for terrestrial plant growth. Floodplains that alternate seasonally between inundation and desiccation, with both conditions presenting stresses that limit the plant life, have been referred to as “hyperseasonal” ecosystems [Sarmiento, 1983]. Savanna floodplains throughout the tropics are important as grazing lands for cattle, and although the seasonal flooding can be an impediment to ranching, the role of flooding in enhancing the production of native pastures and alleviating dry-season stresses is generally recognized [e.g., Wilcox, 1992]. The floodplains with the greatest time lags between rainfall and inundation tend to have less desiccation stress for the plant life during the local dry season.
 The Large Scale Biosphere-Atmosphere Experiment in Amazônia (LBA), an international research initiative led by Brazil, is designed to improve understanding of the physical, chemical and biological functions of the Amazon region, the interactions of those functions with the overall Earth system, and the impacts of changing land use on those functions. In South America, extensive floodplains are important components of the landscape throughout the Amazon River basin as well as in the Orinoco and Paraná river basins [Junk, 1993]. Simulation models of water and material fluxes through riverine systems require information on inundation patterns to account for the hydrological and biogeochemical effects of floodplains [Vörösmarty et al., 1997]. Data on the total area and duration of flooding are required to estimate methane emissions from floodplains, which occur largely during the inundation phase, and South American floodplains are a significant source of atmospheric methane on a global scale [Bartlett and Harriss, 1993; Sahagian and Melack, 1998]. Knowledge of the spatial and temporal variability of inundation in floodplains is fundamental for the conservation and management of floodplain rivers [Junk, 1997; Hamilton, 1999]. Therefore information on inundation patterns in South American floodplains is an integral part of the data requirements for the LBA program.
 Inundation patterns in the major floodplains of South America have remained poorly known because of the vast size and remoteness of these areas and the difficulty of using optical remote sensing technologies such as Landsat in humid regions, where cloud cover limits the ability to acquire multiple images over time. Satellite-borne active radar systems are capable of providing spatially detailed synoptic views of geomorphology and vegetation in floodplain landscapes [Hess and Melack, 1994; Hess et al., 1995], but the temporal coverage by processed radar imagery over the vast floodplains of South America has so far been limited to seasonal mosaics, and hence information on hydrological dynamics has been limited.
 Like radar, passive microwave remote sensing from satellites can reveal the presence of surface water despite cloud cover, but offers the advantage of higher temporal frequency of the available data and more years of data collection. The spatial resolution of passive microwave observations depends on the frequency of measured emission, but is coarse compared to radar. Methods have been developed to estimate flooded area from the 37-GHz polarization difference observed by the Scanning Multichannel Microwave Radiometer (SMMR), operated on board the Nimbus-7 satellite from December 1978 through August 1987. The SMMR observation period coincides with a relatively complete set of stage observations for South American rivers, and that facilitates comparison of the satellite information with ground observations of the timing of flooding. Previous publications have described the methods in detail and presented results for the fringing floodplains of the central Amazon River system and four of its major tributaries [Sippel et al., 1994, 1998], the Pantanal wetland in Brazil [Hamilton et al., 1996; Hamilton, 1999], and the Llanos de Moxos in Bolivia and Llanos del Orinoco of Venezuela and Colombia [Hamilton et al., in press]. Technical issues associated with the geolocational and radiometric accuracy of the SMMR observations as well as the algorithm development for estimation of inundation area and uncertainties in the estimation are addressed in those previous publications (particularly Hamilton et al.  and Sippel et al. ).
 The present study employs the SMMR passive microwave observations in a comparative analysis of inundation patterns among six major floodplains of South America (Figure 1): 1) mainstem Amazon River floodplain in Brazil; 2) Llanos de Moxos in Bolivia; 3) Bananal Island on the Araguaía River in Brazil; 4) Llanos del Orinoco of Venezuela and Colombia; 5) savannas of Roraima State in Brazil and the adjacent Rupununi River of Guyana; and 6) Pantanal wetland, located mostly in Brazil with smaller areas in Bolivia and Paraguay. Data from previous publications on four of these regions are combined with new analyses employing similar approaches to determine inundation patterns in the Bananal and Roraima floodplains. This study provides an unprecedented comparative view of inundation patterns because the satellite observations coincide in time and were analyzed with consistent methodology.
2. Study Sites
 The locations of the six floodplain regions analyzed in this study are depicted in Figure 1, with additional information in Table 1. All of these floodplains lie at low elevations (<250 m) where the climate is tropical and humid, although the precipitation is seasonal. Together these floodplain regions comprise much of the total floodplain area in the continent. In addition, however, there is significant floodplain area along the major tributaries in the Amazon River system [Sippel et al., 1992], along the upper Amazon River mainstem in Peru, along the middle and lower reaches of the Paraná River in Argentina, and in the coastal deltas of the Orinoco, Amazon, and Paraná rivers [Junk, 1993]. The total area of floodplains along smaller river systems is also likely to be significant [Junk, 1993], but has yet to be quantified.
Table 1. Characteristics of the Grid-Cell Aggregates for Each Floodplain Regiona
Number of Grid Cells
Number of Subregions
Northwest Latitude, Longitude
Southeast Latitude, Longitude
The table shows the number of grid cells that were aggregated to encompass the region, the number of subregions for which the calculations were carried out, the empirically determined mean values of ΔTnf and ΔTf (in kelvins; see text for explanation), and the latitude and longitude coordinates defining rectangles that approximately encompass the grid-cell aggregates. The area of a grid cell varies slightly with latitude but is ∼765 km2.
ΔTnf of 6.1 K was used for Roraima unless the 2-month “precipitation excess” (see text) equaled zero, at which time no inundation of the floodplain was assumed.
 The data presented for the Amazon River floodplain represent the floodplain fringing the main stem within Brazil (known as the Solimões and Amazonas rivers), extending from the western Brazilian border (70°W) to the mouth. Tributary floodplains are not included except in the immediate vicinity of confluences. The Amazon River floodplain is largely covered with evergreen forest although more open grasslands become abundant below Santarém [Mertes et al., 1995; Junk, 1997]. The seasonal cycle of river discharge is attenuated by the differential timing of runoff from Andean watersheds as well as lowland watersheds on both sides of the equator [Sioli, 1984]. The mean annual discharge of the Amazon River at Óbidos is 162,000 m3/s [Richey et al., 1989] and the annual fluctuation in stage is 7–10 m. Mean annual precipitation varies across the Amazon Basin, averaging ca. 2300 mm [Vörösmarty et al., 1996]. Details on methods and results for analysis of passive microwave observations of the mainstem Amazon floodplain as well as four of its tributaries can be found in the work of Sippel et al. .
 The Llanos de Moxos (also spelled as Mojos) is a savanna region located in the upper Madeira River watershed in northeastern Bolivia, mostly between the Beni, Mamoré, and Guaporé (or Iténez) rivers. In this region, the natural vegetation tends to be evergreen forest in areas that are not subject to seasonal inundation, and inundation tends to maintain grassland or savanna vegetation [Langstroth, 1996]. The Beni and Mamoré rivers drain montane watersheds of the Andes and carry mean annual discharges of 9000 and 8400 m3/s, respectively, while the Guaporé River drains lower elevations to the east in Bolivia and Brazil and carries a mean annual discharge of 2100 m3/s [Guyot and Wasson, 1994]. River discharge is strongly seasonal and results in large fluctuations in water level, reaching 11 m in the Mamoré River channel, although the river channels are incised into the plains and the depth of inundation in most of the savanna areas remains <1 m [Hanagarth, 1993]. Mean annual precipitation varies from 1300 to 2000 mm across the region, occurring mostly between September and May [Hanagarth, 1993]. Details on methods and results for analysis of passive microwave observations of the Moxos region can be found in the work of Hamilton et al. [in press].
 The Bananal floodplain is located in east-central Brazil along the Araguaía River, a tributary of the Tocantins River. Much of this floodplain is on the Bananal Island, which lies between two anabranches of the Araguaía River, but there is also extensive contiguous floodplain upriver of the island to 15°S latitude. The Araguaía River carries a mean annual discharge of 1680 m3/s. The floodplain vegetation is largely savanna [Eiten, 1985], while surrounding uplands tend to be covered by tropical moist forest to the north and west and savanna (much converted to agriculture) to the south and east. Annual rainfall averages 1700 mm and is strongly seasonal. The Araguaía River stage varies by about 5 m over the seasonal cycle, but most of the floodplain is inundated to only 1–2 m depth or less [Eiten, 1985].
 The Llanos del Orinoco is a region of alluvial plains between the Orinoco River and the Andean foothills. The climate here tends to support savanna vegetation regardless of whether seasonal inundation occurs [Sarmiento, 1983], but in this study the Llanos del Orinoco region is defined as the lower-lying savanna areas that are subject to seasonal inundation. The floodplains of this region are drained by two major tributaries of the Orinoco River, both of which originate in the Andes: the Apure River (mean annual discharge, 2300 m3/s) and the Meta River (5600 m3/s) [Lewis et al., 1995]. The Orinoco mainstem fluctuates by 10–15 m over the annual cycle, but tributary stage fluctuations are lesser within the Llanos where the floodplains absorb the excess discharge. Mean annual precipitation in the region is about 1500 mm and is strongly seasonal. Details on methods and results for analysis of passive microwave observations of the Llanos del Orinoco can be found in the work of Hamilton et al. [in press].
 The floodplains of Roraima include the savanna areas of Roraima State in northern Brazil as well as the contiguous Rupununi savannas of Guyana. Most of this territory lies within the watershed of the upper Branco River, a tributary of the Negro River that carries a mean annual discharge of 2900 m3/s at the outflow from the region. The Rupununi savannas lie in the watershed of the Rupununi River, a smaller river that flows north into the Essequibo River. As in the Llanos de Moxos, the presence of savanna in this region tends to indicate seasonal inundation while areas without seasonal inundation tend to be evergreen forest, although human activities may have increased the extent of grassland at the expense of forest. Floodplain vegetation includes nearly treeless grasslands as well as Mauritia palm swamps [Beard, 1953; Sarmiento, 1983]. Much of the savanna floodplain is associated with several smaller tributary rivers that have distinct upland watersheds, including the Surumu and Parime rivers. The seasonal fluctuations in stage of these tributary rivers are unknown; the Branco River at Boa Vista varies by about 6 m over the annual cycle. Rainfall averages about 1700 mm and is highly seasonal, with a marked dry season.
 The Pantanal wetland is located on the upper Paraguay River, mostly in Brazil with smaller areas in Bolivia and Paraguay. The Pantanal is a complex of river floodplains lying in a vast sedimentary basin filled by the deposition of alluvial fans from several tributaries. Inundation patterns in the region vary depending on the source of floodwaters (e.g., overbank flow from rivers vs. delayed drainage of precipitation) as well as backwater effects due to the limited capacity of the river channels to convey the seasonal floodwaters [Hamilton, 1999]. The Paraguay River drains the region and flows south to the Paraná River; in the southern Pantanal the river carries a mean annual discharge of ca. 2500 m3/s and fluctuates in stage by about 5 m. The Pantanal supports a variety of savanna and emergent marsh vegetation; upland areas that are not subject to inundation are generally savanna vegetation although much has recently been converted to agriculture. Environments of the Pantanal are described in the works of Junk and da Silva , Por , and Heckman . Annual rainfall is 1000–1500 mm and is seasonal. Details on the methods and results for analysis of passive microwave observations of the Pantanal can be found in the work of Hamilton et al. .
3.1. SMMR Data Characteristics
 The SMMR instrument measured the natural emission of microwave energy from the Earth's surface and atmosphere. Measurements are expressed as brightness temperatures (in Kelvins), and are available at several frequencies and at both vertical and horizontal polarizations [Fu et al., 1988]. The difference between vertically and horizontally polarized brightness temperatures observed by satellite at the 37 GHz frequency (hereafter referred to as ΔTobs) provides a sensitive indicator of the presence of surface water, particularly where water occurs against a background of vegetated land surfaces. Choudhury  reviewed the theoretical basis for interpretation of 37-GHz emission. The spatial resolution of the SMMR sensor is approximately 27 km at 37 GHz and the processed global data set is gridded into cells of 0.25° latitude by longitude.
 Satellite observations of 37-GHz emission are available for December 1978 to August 1987 from the SMMR instrument operated on board the Nimbus-7 satellite [Gloersen et al., 1984; Fu et al., 1988]. This study uses the monthly SMMR observations originally described by Choudhury [1989, 1991]. Global SMMR observations are available for approximately 6-day intervals, and are compiled separately for day and night (local equator crossings at noon and midnight). After calculation of ΔTobs for each grid cell from the daytime brightness temperatures, the observations were ranked within each month and the second lowest value (out of 4 or 5) was selected, thereby yielding one ΔTobs value per month [Choudhury, 1989]. This screening served to eliminate outlying values that might have resulted from atmospheric scattering by heavy rainfall, or from temporary pooling of water on the land surface after heavy rainfalls.
3.2. General Approach
 The approximate boundaries of the floodplains were delineated using maps, remote sensing, and scientific publications, and by examination of the SMMR data for evidence of inundation. In the Llanos de Moxos, Llanos del Orinoco, and Pantanal, the subregions correspond approximately with hydrogeomorphic provinces (Table 1), although the subregion boundaries are dictated by the coarse resolution of the SMMR data. The boundaries were altered in some cases to avoid crossing or bordering major open-water features such as the largest floodplain lakes or river channels. In the cases of the Amazon and Bananal floodplains, subregions reflect arbitrary subdivisions along the direction of river flow, and the Roraima floodplains were analyzed as a single region because of their relatively small extent. Regional and subregional boundaries were chosen to encompass the floodplain subject to inundation and therefore include some upland area along the outer edges.
 Our general approach to determine inundation area from the SMMR ΔTobs has been described in detail in the works of Hamilton et al.  and Sippel et al.  and will only be briefly summarized, with additional site-specific details provided for the new data that are presented. The fractional inundation area within an aggregate of SMMR grid cells was estimated using linear mixing models that account for the microwave emission of the major landscape units, or end-members, within the subregion [Sippel et al., 1994]. The model has three end-members that represent the contributions of water, nonflooded land, and inundated floodplain to the ΔTobs:
where ΔTobs is the ΔT observed by the radiometer, fw, fnf and ff are the fractional areas of open water (rivers and lakes without emergent vegetation), nonflooded land, and seasonally flooded land, respectively, and ΔTw, ΔTnf, and ΔTf are the ΔT values for open water, nonflooded land, and seasonally flooded land. Simultaneous solution of equations (1) and (2) yields the following equation for the fraction of inundated floodplain (ff):
The fractional area of open water is assumed to vary little over the annual cycle, and is measured from maps or remote sensing imagery. The fractional area of flooded land expands during inundation with a concomitant reduction in the fractional area of nonflooded land, which includes nonflooded floodplain as well as any upland area within the grid-cell aggregate. The ΔT values for end-members in these models, which are summarized in Table 1, were determined as follows.
 The ΔTnf values for nonflooded land were determined empirically by examination of the ΔTobs measured over floodplain areas in the driest periods, as well as examination of ΔTobs measured over upland areas with comparable vegetation cover. The ΔTw value for open water cannot be determined empirically in most of these floodplain regions because the fractional coverage by open water is small, but this value is not expected to vary for calm water surfaces. In most cases a theoretical value of 60 K was used [Choudhury, 1989]; the ΔTw value was determined empirically only in the Amazon floodplain where the fractional coverage by open water is large enough to do so [Sippel et al., 1998].
 The ΔTf values for flooded land were determined empirically for each region (except Roraima; see below) because they are expected to vary, primarily as a function of the density and structure of vegetation canopies overlying the water. Within a region, the ΔTf could be expected to vary over the seasonal cycle of water level change, but variability in the proportion of water surface overlain by plant canopies is reduced because tree canopies generally remain emergent during inundation and herbaceous aquatic vegetation is generally composed of floating mats that rise and fall with the water level. The empirical determination was done at maximum inundation, representing the approximate midpoint of the inundation cycle. All available sources of information were considered to select calibration cells in each subregion, which are SMMR grid cells that are entirely subject to inundation in most years and can be used to determine the ΔTf value under conditions of complete inundation [Sippel et al., 1994]. The ΔTf values from the calibration cells were averaged to yield a single estimate of ΔTf unless there was a discernible spatial pattern in their variation.
 The fractional inundation area was calculated for each monthly ΔTobs observation using equation (3), and inundation areas of the subregions were summed to yield the total inundation area for the region. Inundation area includes the permanent open-water area of river channels and floodplain lakes unless noted. Concurrent data on river levels (stage) from sites with long records were examined to produce predictive relationships between river stage and flooded area for each region. Mean monthly stage was computed, and cross-correlation analyses between the time series of stage and flooded area served to check for time lags of one month or more. Polynomial regression analysis yielded predictive equations to extend the inundation record over the period of river stage observations; such nonlinear predictive equations must not be employed outside of the range of stage data from which they were established.
3.3. Site-Specific Methods for Bananal and Roraima
 The analysis of passive microwave observations for the Bananal and Roraima floodplains has not been reported previously. Unless noted, the methods for these two floodplains are similar to those detailed for the Moxos and Orinoco floodplains in the work of Hamilton et al. [in press].
 The grid-cell aggregates for the Bananal floodplain were delineated by including all contiguous grid cells that had a standard deviation ≥1.5 K during the 9 years of ΔTobs observations. The Bananal region extends between 9°15′ and 15°S latitude along the Araguaía River. In the Roraima region, some grid cells to the north and west of the savanna region showed elevated standard deviations for ΔTobs that suggested seasonal flooding of forested wetlands. The grid-cell aggregate was confined to the contiguous savannas of the region, as depicted in the work of Sarmiento . The boundaries for both regions were then confirmed by comparison with independent sources of information: 1) the floodplain maps produced from Side-Looking Airborne Radar by the RADAMBrasil project and reproduced in the work of Junk , 2) 1:250,000-scale topographic maps produced by the Brazilian government, 3) low-water Landsat images, 4) JERS radar mosaics from the National Space Development Agency of Japan, and 5) an image depicting the Normalized Difference Vegetation Index derived from the NOAA Advanced Very High Resolution Radiometer. The Bananal floodplains were arbitrarily subdivided into three subregions along the north-south axis because of a time lag in the passage of the flood peak from south to north; the divisions were made at 11°15′ and 13°15′S latitudes. The less extensive Roraima floodplains were analyzed as a single region.
 The permanent open-water area of river channels and lakes was measured from classified Landsat images. The river channels in these dry-season images showed areas of sandbars that were not classified as open water, and thus open water at higher river stages may be larger. However, the fractional open-water area is not large in the Bananal and Roraima regions (Table 1) and therefore this is not important source of error in our analysis. Floodplain lakes are numerous in these regions but they tend to be very small, and hence there is little open water area outside of the river channels in these two floodplain regions.
 In previous work in the central Amazon floodplain and in the Pantanal region, upland areas covered by savanna or forest vegetation were observed to have a mean ΔTnf of ca. 4.2 ± 1.0 K (mean ± s.d.) throughout the year [Sippel et al., 1994; Hamilton et al., 1996, in press]. This is close to the value expected as a result of attenuation of the microwave emission by vegetation canopies that completely cover the soil [Choudhury, 1989]. Examination of dry-season ΔTobs values as well as information on vegetation coverage during the dry season indicate that 4.2 K is the appropriate ΔTnf for the Llanos de Moxos and Bananal floodplains. However, in nonflooded savanna regions where soils are exposed among vegetation, Justice et al.  noted slightly elevated ΔTobs values, probably because the attenuating effect of the vegetation on emission from underlying soils is reduced. This phenomenon does appear to occur in the Llanos del Orinoco, where a significant increase in the ΔTobs during the course of the dry season was observed in some upland and floodplain savannas. This increase was most likely due to increasing exposure of sand and lateritic crusts as the vegetation became sparser, and hence the ΔTnf increased over time [Hamilton et al., in press].
 As in the Orinoco, a dry-season increase in ΔTnf is apparent in the Roraima region, where there was a tendency for the ΔTobs to increase over the course of the dry season from about 6–7 K to 7–8 K. This increase could not be explained by flooding because monthly rainfall totals for the two stations in the region show no significant excess over the likely rate of evapotranspiration, and the river stage remained low during the dry season. The presence of exposed sandy and stony surfaces as well as the severity of the dry season have been noted in the literature on the Roraima savannas [Beard, 1953; Sarmiento, 1983], and a dry-season decrease in grassland vegetation canopies could increase the exposure of underlying soils, increasing the ΔTobs. Therefore for calculation of inundation area, it was assumed that there was no inundation outside of open-water areas during month t whenever there was a “precipitation deficit” that lasted for two months, as defined by a mean monthly rainfall for months t and t-1 below 120 mm, which is a conservative estimate of monthly evapotranspiration in the region [Hills, 1968; Salati, 1985]. Rainfall data are means for two rainfall measurement stations, one at Boa Vista (2°49′47″N, 60°39′42″W) and the other at Fazenda Passarão (3°12′28″N, 60°34′16″W). A ΔTnf = 6.1 K was used for the calculation of fractional inundation area on the remainder of the dates, which was the mean ΔTobs value observed early in the dry seasons, corrected for the permanent open-water contribution.
 The ΔTf value for Bananal was determined empirically from a set of 12 calibration cells, as was done previously for the other floodplains. The relatively small Roraima region does not have large homogeneous expanses of floodplain that fill entire grid cells, and thus the ΔTf could not be determined empirically there. Therefore the algorithms for Roraima employ the mean ΔTf value for 39 calibration cells in the 4 subregions of the Llanos del Orinoco that most closely resemble the savannas of Roraima (excluding the more deeply flooded Apure Delta subregion).
 Relationships between mean monthly river stage or rainfall and flooded area were evaluated using the closest river stage or rainfall stations that had long records. Stage and rainfall data were obtained from the Brazilian Agência Nacional de Energia Elétrica (ANEEL). For the Bananal floodplain, there was a good correlation between flooded area and the Araguaía River stage at Luiz Alves (13°12′35″S, 50°35′6″W). For the Roraima floodplain, there was a good correlation between flooded area and the stage of the Branco River at Boa Vista (2°49′47″N, 60°39′42″W), which is located downriver of most of the floodplain. Compared to river stage, rainfall was not as well correlated with floodplain inundation area in either floodplain region.
4. Results and Discussion
4.1. Passive Microwave Observations of Inundation Area
 Time series of the total flooded area in each of the regions show considerable variability in the total extent of inundation in these floodplains, both seasonally as well as interannually (Figure 2). This variability is easier to visualize as a dot plot depicting the distribution of the annual minima and maxima (Figure 3). The maximum extent of inundation is variable among years in all of these floodplains, with the greatest relative variation in Bananal and Roraima. In most cases nearly all of the land that was subject to seasonal inundation became dry each year. The Pantanal appears to retain the most flooded area at low water, but this is due to the long time lag (4–6 months) for passage of the flood across the region; most individual subregions become largely dry in most years [Hamilton et al., 1996].
 In floodplains where there are time lags for the passage of the flood across the region, the total area of land subject to inundation is larger than the maximum area of simultaneous inundation. Table 2 shows both the maximum area that was simultaneously flooded and the maximum area subject to flooding in at least one month of the calendar year. Using the latter area as a definition of floodplain extent, the Pantanal is the largest floodplain (130,920 km2), followed by the Llanos del Orinoco (107,530 km2). Roraima is the smallest of the floodplains analyzed, and is the only region that appears to dry completely for several months each year (except for river channels and small permanent floodplain lakes).
Table 2. Summary Statistics of the Inundation Area Estimates (km2) for the Six Floodplain Regions During the Period of SMMR Observations (1979–1987)a
The open-water area of rivers and lakes is included in the flooded areas. The maximum simultaneously flooded area is the maximum observed in the monthly time series of total flooded area for the region, whereas the maximum area subject to flooding is the sum of the maximum areas attained in each subregion (or individual grid cell, in the case of the Pantanal). The area subject to flooding tends to be larger because of temporal differences in flooding across the regions; for Roraima, it is the same as the maximum area simultaneously flooded because the analysis was done as a single region. The floodplain hydroperiod is defined here as the frequency at which the floodplain was inundated to ≥50% of its maximum inundation area over 9 years of observations; permanent open-water areas of rivers and lakes were subtracted from the floodplain area to determine hydroperiod.
Open-water area (rivers and lakes)
Maximum area simultaneously flooded
Maximum area subject to flooding in a calendar year
Mean flooded area, 1979–87
Long-term mean flooded area as estimated from stage records (time period)
Floodplain hydro-period (days per year)
 The timing of flooding and drainage also varies among the four regions, as depicted by the mean flood hydrographs (Figure 4). The variable timing of inundation reflects the local wet and dry seasons, which are different on either side of the equator. The Amazon River receives its discharge from subbasins on both sides of the equator, resulting in a less marked seasonal cycle. Comparison of the mean seasonal cycles of rainfall and inundation shows how each region except for Roraima has a time lag of variable duration between rainfall in the watershed and flooding on the floodplains. The Amazon, Llanos de Moxos, and Pantanal tend to reach peak inundation 2–3 months after the height to the local wet season and retain substantial flooding during the local dry season, while flooding of the Bananal, Llanos del Orinoco, and Roraima floodplains is more synchronous with the local wet season. Perhaps the most dramatic example among the six floodplain regions is the Pantanal, where inundation in the southernmost subregions can occur at the peak of the local dry season, producing a verdant floodplain when adjacent upland soils are dry, grasslands are brown, and many trees have shed their leaves. As the flood waters recede the rains tend to increase and terrestrial vegetation thrives, in contrast to floodplains such as Roraima where the rainy season is nearly synchronous with floodplain inundation and the dry season is a time of limited water availability in much of the floodplain.
 Flood duration curves shown in Figure 5 reveal characteristic patterns for each floodplain and can be used to estimate exceedance frequencies, as is commonly done with river discharge. One way to consider the duration of floodplain inundation (or floodplain hydroperiod) is to use the flood duration curves to determine the frequency at which the floodplain was inundated to ≥50% of its maximum inundation area over the 9 years of observations, and to express this frequency as the average number of days per year (Table 2). The hydroperiod as defined here applies only to the seasonally inundated floodplain, and thus the permanent open-water area of rivers and lakes has been subtracted for determination of the 50% inundation exceedance frequencies. These hydroperiod estimates show considerable variation, ranging from a maximum of 172 days for the Pantanal to only 57 and 49 days for the Bananal and Roraima floodplains, respectively. The duration of the hydroperiod is positively correlated with the total area of seasonally inundated land, reflecting the tendency for more protracted flooding in larger floodplains where the flow paths for drainage of floodwaters to the rivers are longer (Figure 6).
4.2. Extension of the Inundation Record
 The relationships between flooded area derived from passive microwave remote sensing and ground observations of river stage reveal the degree to which floodplain inundation is linked to water level in the major rivers associated with the floodplains. This information is increasingly needed to assess the environmental impact of river channel modifications, including impoundments as well as navigation projects. For example, Hamilton  examined stage/flooded area relationships for subregions of the Pantanal to show how inundation of much of the floodplain is directly linked to water levels in the rivers. A correlation between river stage and flooded area does not necessarily imply control of flooding by the river level at that measurement station, however, as exemplified in the cases of the Moxos and Orinoco floodplains where the selected stage stations are located far downriver of the floodplain regions.
Figure 7 depicts the stage/flooded area relationships and Table 3 summarizes the predictive equations to extend the inundation record over the longer time period for which river stage observations are available. The relationship between flooded area and stage tends to be nonlinear because at lower stages the rivers are confined within their banks, while at higher stages the river increasingly establish connectivity with their floodplains and flooded area increases rapidly with stage. At flood stages, the stage/flooded area relationship is determined by the floodplain geomorphology as well as time lags for filling and drainage of the more extensive floodplains. Time lags may also exist when the stage measurement station is downriver of much or all of the floodplain, as is the case for the Llanos de Moxos, Llanos del Orinoco, and the Pantanal. If the time lags are approximately one month or greater, a better relationship can be obtained by incorporating a lag into the regression, which was done for the Roraima and Pantanal floodplains. In cases where distinct relationships with flooded area were observed at rising and falling stages, separate predictive equations were employed.
Table 3. Empirical Relationships to Predict Flooded Area From River Stagea
Floodplain Region (No. of Data Pairs)
River Stage Station (River Name)
Range of Stage (1979–1987), m
Flooded area includes open water area of lakes and rivers. These equations are derived from the data in Figure 7 and can be employed to extend the inundation record over the period of stage observations, provided that the stage remains within the range of the 1979–1987 period. The coefficients of determination (R2) provide an indication of the degree to which water levels in the major rivers associated with these floodplains reflect the extent of seasonal inundation. Time lags were incorporated when they improved the prediction; for example, a lag of 1 month means that the predictive relationship employed the mean river stage from the following month to predict mean flooded area in a particular month. The regressions of inundated area (Y, in km2) on stage (X, in m) take the form of Y = A + BX + CX2 + DX3.
For the Pantanal, the regression uses the mean stage of the following 2 months because of the long time delay for passage of the flood across the region and the downstream location of the stage station [Hamilton et al., 1996].
 The extended records of inundation depicted in Figure 8 provide a better indication of interannual variability than the 9-year SMMR time series, even though the regression technique does not capture the full range of variability in maximum and minimum flooding extent [Moog et al., 1999]. Long-term means for inundation area in these extended records resemble the means for the 9-year SMMR period, except for the Pantanal where the long-term mean is considerably lower (Table 3). The mean and coefficient of variation for the maximum annual inundation areas in each of the extended series are given in Table 4. A marked flood pulse occurred in the Amazon and Orinoco floodplains in nearly all years, resulting in the lowest coefficients of variation in Table 4. In contrast, the Pantanal shows the greatest interannual variability in maximum inundation, with a tendency for multi-year periods of drier or wetter conditions and some years with relatively little flooding. Occasional protracted dry periods with little flooding, as for example in the Pantanal from 1960 to 1973, strongly impact wildlife populations, produce changes in floodplain vegetation, and can result in the expansion of human activities on the floodplain. Records for the Bananal and Roraima floodplains are shorter but also show considerable variability in the magnitude of the flood pulse. The Llanos de Moxos inundation record, extending back to 1967, shows somewhat less variability in the maximum inundation. In the years 1967–1973, when the Pantanal was in the latter part of a protracted drought, the Moxos floodplains were evidently still subject to substantial flooding, albeit less than in subsequent years. The interannual variability in inundation in these regions is caused by climatic variability that is driven in part by sea surface temperature anomalies in the tropical Pacific Ocean [Hastenrath, 1990; Robertson and Mechoso, 1998].
Table 4. Means for the Maximum Annual Inundation Over the Extended Records Depicted in Figure 8.a
Long-Term Mean (km2) and c.v. (%) of Maximum Annual Inundation
No. of Years in Record
Inundation area includes the permanent open waters of rivers and lakes (open-water areas are given in Table 1). Variability in maximum annual inundation is expressed as the coefficient of variation of the mean (c.v., in %).
Llanos de Moxos
Llanos del Orinoco
 Information on the mean annual inundation area is required to estimate rates of trace gas exchange between tropical wetlands and the atmosphere. The lack of data on the mean flooded area for each of the major tropical wetlands has limited the accuracy of these estimates. For example, previous attempts to estimate methane emission rates have assumed that tropical floodplains were fully inundated for 50% of the year, which is equivalent to a mean inundation area of 50% of the total area [e.g., Matthews and Fung, 1987; Bartlett and Harriss, 1993], or they have assigned an average duration of inundation for different categories of wetlands based on site-specific studies [Aselmann and Crutzen, 1989]. The aforementioned studies also differ substantially in the total areas of South American wetlands used in the calculations. Comparison of the long-term mean annual inundation area to the total area subject to inundation in Table 2 shows that the mean inundation area ranges between 22–48% of the total area (five of the six range 22–32%). The higher inundation percentage for the Amazon floodplain is due to the larger fraction of permanent open waters. These results show that the assumption of 50% inundation leads to overestimation of methane emission rates by nearly two-fold in wetlands that are largely composed of seasonally inundated lands, which are the most extensive kind in South America. Aselmann and Crutzen  assumed that “seasonal floodplains” were inundated for 3.5 months per year (equivalent to 29% mean inundation), which is quite close to the results reported here. The total floodplain areas reported here are also similar to those used by Aselmann and Crutzen , based on information from diverse sources that was originally compiled and eventually published by Junk .
5. Conclusions and Future Work
 The SMMR observations of passive microwave emission have provided new insights into the dynamics of inundation in these vast floodplains, which is fortuitous considering that the sensor system was not designed for observation of flooding [Choudhury, 1989]. The fluctuations in flooded area could be characterized despite the coarse spatial resolution of the sensor system because of the large extent of these floodplains. Smaller floodplains or those with more erratic fluctuations in flooded area would be more difficult to study using the SMMR observations and would require sensor systems with greater spatial resolution as well as new ground observations for calibration and validation.
 Additional satellite observations of passive microwave emission have been made by the Special Sensor Microwave Imager since the SMMR deployment ended in 1987, as part of the Defense Meteorological Satellite Program [Hollinger et al., 1990]. New sensor systems such as the Conical Microwave Imager Sounder [Flaming, 2000] should maintain continuity in the global record of passive microwave emission measurements. Correction for atmospheric interference is increasingly feasible and should reduce the variance in the measurements [Choudhury et al., 1992; Prigent et al., 1997, 1998]. In addition, other remote sensing approaches such as synthetic aperture radar [Hess et al., 1995] and radar altimetry [Birkett, 1998] have begun to produce complementary information on these floodplains. Challenges that lie ahead include calibration and validation of the newer passive microwave sensor systems to yield a continuous record of comparable inundation observations, and the synergistic combination of the information on inundation patterns from passive microwave emission with data on geomorphology, vegetation, and water levels that are increasingly available from other kinds of remote sensing systems.
 This research was based upon work supported by the U.S. National Aeronautics and Space Administration under grants NAGT 30013, NAGW-2724, NAGW-4352, NCC5-281, and by the National Science Foundation under grant DEB-9701714. Numerous local and international scientists assisted with our research and contributed to our comprehension of these floodplain regions, but we especially wish to acknowledge the support of the staff of the Pantanal research center operated by the Empresa Brasileira de Pesquisa AgropecuÃria. We also acknowledge the Agõncia Nacional de Energia ElÕtrica, the Brazilian Navy, and the firm Hidrologia SA for the Brazilian stage and rainfall data, and the Venezuelan Ministerio del Ambiente y de los Recursos Naturales Renovables for the Orinoco River stage data. This research was greatly enhanced by the efforts of anonymous citizens and government employees who faithfully maintained river stage observations over many decades. D. Skole and W. Chomentowski of the Basic Science Remote Sensing Initiative at Michigan State University (a NASA Earth System Information Partner) provided the Landsat imagery and assistance with its analysis, D. Moog offered statistical advice, E. M. M. Novo assisted with the Amazon work, and L. Hess provided JERS radar mosaics and commented on the manuscript. This is contribution 962 of the W. K. Kellogg Biological Station.