The Fate of Carbon in Sediments of the Xingu and Tapajós Clearwater Rivers, Eastern Amazon

Introduction

Recent research has undermined the view of rivers as passive conveyors of organic matter, and demonstrates their role in the transport, modulation, and deposition of carbon (Cole et al., 2007; Tranvik et al., 2009; Aufdenkampe et al., 2011; Ward et al., 2015). Inland waters emit at least 0.8 Pg of carbon per year (Cole et al., 2007; Tranvik et al., 2009). Approximately one fourth of it comes from rivers (Cole et al., 2007). The Amazonian rivers represent about 15% of the terrestrial gross primary production and 25% of the global rivers emissions of CO₂ (Field, 1998; Richey et al., 2002). Most studies that have considered organic matter remineralization and carbon storage in the region focused on the Amazon mainstem and its floodplains (Richey et al., 2002; Bouchez et al., 2010, 2012; Abril et al., 2014; Ward et al., 2015). However, the lack of geochemical data to constrain the role of major clearwater tributaries of the Amazon River as a source or sink of organic sediments limited the understanding of the carbon cycling dynamics across the terrestrial and aquatic environments of the Amazon basin.

The Xingu and Tapajós rivers represent the largest Amazon clearwater rivers, with mean annual discharges of 9,700 and 13,500 m³s⁻¹ (Latrubesse et al., 2005), respectively. They drain crystalline and sedimentary rocks of the Central Brazil shield and are characterized by relatively low concentrations of suspended sediments, slightly alkaline waters (Sioli, 1984), and high fluxes of methane to the atmosphere (Sawakuchi et al., 2014). Both rivers are naturally impounded by the Amazon mainstem, which give rise to broad downstream lake-like channels known as “fluvial rias” (Gourou, 1949; Archer, 2005). The Xingu and Tapajós rivers have strong seasonal variations, with mean monthly water discharges varying from approximately 1,000 to 20,000 m⁻³ s⁻¹ in the Xingu River and 4,000 to 30,000 m⁻³s⁻¹ in the Tapajós River (ANA, 2016). The peak discharges of these clearwater rivers occurs from February to May. The Amazon River, however, has a mean monthly water discharge that varies from approximately 105,000 m⁻³ s⁻¹ to 235,000 m⁻³ s⁻¹, with peak discharge from April to July (ANA, 2016). The lag between the peak discharge of the Amazon River and its clearwater tributaries is responsible for strong backwater effects in the Xingu and Tapajós rivers (Meade et al., 1991). The sudden drop in water flow velocity and channel widening related to the hydraulic blockage and backwater effect by the Amazon mainstem prevent most of the Xingu and Tapajós suspended and bedload sediments from entering the Amazon River. These conditions turn rias into massive sinks for organic and inorganic sediments and natural reactors for carbon derived from the headwaters. Fluvial rias in the downstream section of the Xingu and Tapajós rivers reach up to 15 km width and around 150 km length. Hundreds of rias and paleo-rias occupy the Amazonian landscape and connect all clearwater and blackwater tributaries to the Amazon River, playing an important role for the transport and deposition of fine-grained sediments in the Amazon fluvial system. Thus, the accumulation of fine-grained sediments in rias has a strong effect on carbon processing and transport to the Amazon River and the Atlantic Ocean. To date, studies addressing Amazonian fluvial rias focus mainly on climatic and sediment deposition changes, without consensus about their genesis (Sioli, 1984; Keim et al., 1999; Vital and Stattegger, 2000; Bertani et al., 2014). The extant Amazon rias appear to have been formed after the Last Glacial Maximum (LGM, 23–19 ka) (Archer, 2005; Irion et al., 2011). The prevailing hypothesis suggests that the incised valleys formed during the low sea level phase of the LGM were flooded and accumulated sediments during the Holocene transgression (Archer, 2005; Irion et al., 2006, 2011). Sediment cores retrieved from the Tapajós Ria contain fine-grained sediments with 2.2–3.5% of total organic carbon and sedimentation rates reaching up to 6.5 mm yr⁻¹ (Irion et al., 2006). This reinforces the potential of rias as location of sediment deposition and carbon processing in the Amazon fluvial system.

Rias show sedimentary dynamics similar to that of lakes and reservoirs, which bury more than 200 Tg of organic carbon annually (Dean and Gorham, 1998). Despite the widespread distribution in the Amazon and dominance of organic-rich sediments (Irion et al., 2011), rias are poorly studied with respect to their role as sink or source of carbon in the Amazon basin. According to Sawakuchi et al. (2014), methane fluxes in Amazon rivers account for 22–28% of the global river emissions of methane and the Amazon rias are hotspots of methane production. Rias also serve as analogs for carbon processing in artificial reservoirs like the recently build reservoirs of the Belo Monte hydropower plant in the Xingu River and future reservoirs planned for the Tapajós River (Winemiller et al., 2016). Clearwater Amazon rivers are the main target in the energy expansion plans of the Brazilian government (EPE/MME, 2007), which regards hydropower as inexpensive and clean energy, however, without consideration of impacts of river impoundment on Amazon ecosystems (Fearnside, 2014; Winemiller et al., 2016) and emission of greenhouse gases (Barros et al., 2011; de Faria et al., 2015). To assess the combined effect of carbon fluxes in Amazon rivers, it is imperative to fully understand carbon burial and emission rates in all main Amazon sedimentary environments. In this paper, we focus on carbon dynamics in the rias of the Xingu and Tapajós rivers. Geochemical, magnetic susceptibility, pollen, and diatom analyses combined with luminescence and radiocarbon dating are used to constrain the sources and fate of carbon in sediments of the Xingu and Tapajós rivers on millennial timescales. We integrated our data and results from previous literature to evaluate the origin and content of organic matter and to understand major controls affecting carbon burial in the Xingu and Tapajós rias.

Materials and Methods

Sediment Sampling

Sediment cores and samples of riverbed and suspended sediments collected from Xingu, Tapajós and Amazon rivers are presented in Figure 1 and in Supplementary Material (Table S1). Suspended sediment samples were taken both during the dry and wet seasons from Xingu, Tapajós, and Amazon rivers in order to fully encompass variations in sediment composition related to hydrological changes. Suspended and riverbed sediment samples from the Amazon mainstem were collected upstream and downstream the Tapajós and Xingu rivers mouths (Figure 1) in order to evaluate the effect of input of sediments from the Xingu and Tapajós rivers on the Amazon River. Suspended sediment samples were collected through water pumped at approximately 60% of the water depth in the channel thalweg. For each sample, four liters of water were filtrated using cellulose acetate membranes (pore size of 0.45 μm). Riverbed sediments were collected using a Van Veen grab sampler. A total of 23 suspended sediment samples and 28 riverbed sediment samples were used in this study.

FIGURE 1

Figure 1. Study area, location of sediment samples (suspended, riverbed and cores) and bathymetric profiles. In this work, underwater sediment cores were named “XC” and sediment cores from islands were named “EMB.” Land-use map from Almeida et al. (2016).

Sediment cores of the Xingu Ria were collected from deeper portions of the lake-like channel covered by muddy sediments (named “XC”) and from islands in the upstream section of the Xingu Ria (named “EMB”). The locations were selected based on water depth profiles and riverbed sediment sampling (further details in Sawakuchi et al., 2015). Underwater sediment cores from the Xingu Ria channel were retrieved by divers using PVC tubes of up to 6 m in length and percussion method (Sawakuchi et al., 2015). Three underwater sediment cores, characterized by dark gray to brown muds with thicknesses of 300 cm (XC02), 370 cm (XC03), and 470 cm (XC05), respectively, were retrieved from the Xingu Ria. Unconsolidated sediments from islands of the Xingu Ria head were collected using a piston-corer attached to a manual auger. Four sediment cores composed of fine to medium sands and muddy organic sediments were obtained from the islands: EMB13-07 (555 cm), EMB13-13 (430 cm), EMB13-17 (250 cm), and EMB13-21 (345 cm). Samples for luminescence dating were collected using opaque plastic tubes.

Bathymetric profiles were recorded along the upstream part of the Xingu Ria using sonar and GPS equipment. Samples collected with the Van Veen grab sampler were used to characterize riverbed sediments along bathymetric profiles. Water depth profiles and texture of riverbed sediments of the Xingu Ria are shown in Figure 2.

FIGURE 2

Figure 2. Bathymetry and riverbed sediment texture in the upstream sector of the Xingu Ria.

Organic and Inorganic Geochemistry of Sediments

Total organic carbon (TOC) content and its stable carbon isotope ratios (δ¹³C_org) were measured in 28 riverbed sediments samples at MARUM, University of Bremen. Sediments from the core XC05 were sampled at 2 cm intervals for total carbon coulometric and x-ray fluorescence (XRF) analysis at the University of Kentucky.

Major elements (P, Ca, Fe, Mn, Al, Ti, K) concentrations were determined with an Agilent 720 inductively coupled plasma—optical emission spectrometer (ICP-OES) for 23 samples of suspended sediments and with a Bruker Tracer IV SD energy dispersive x-ray fluorescence (XRF) spectrometer for 13 riverbed sediments samples and 234 samples of the sediment core XC05. ICP-OES analysis of suspended sediments and XRF analysis of riverbed sediments were performed at MARUM, University of Bremen. For ICP-OES analysis, digestion of suspended material was performed with a MLS 1200 MEGA microwave system. For this purpose, 7 ml HNO₃ (65%), 0.5 ml HF (40%), 0.5 ml HCl (30%), and 0.5 ml MilliQ were added to about 50 mg sample material (filter plus suspended material) previously placed into Teflon liners. All acids were of supra-pure quality. For XRF analysis, sediments were prepared by freeze drying, grinding by hand with an agate mortar and pestle, and sieving to ~125 μm prior to packing into inert sample boats sealed with an ultra-thin mylar window. Individual XRF scans for each sample were made through the mylar window over 90 s, in order to maximize signal-to-noise. Major elements (atomic numbers 11 through 30) were collected under a ~9 torr vacuum, by setting the XRF filter to 15 keV and 35 μA. Trace elements (atomic numbers 20 through 51), were collected at 40 keV and 15 μA without a vacuum. Calibration of unknowns utilized Bruker proprietary software (S1CALPROCESS with TR2.cfz and MA1.cfz) and a reference catalog of mudrock chemistry described in Rowe et al. (2012). Internal consistency of the XRF was verified by routine scanning of the SARM41 shale standard (Ring, 1989). The chief focus of our analysis was the major rock-forming (Al, Ca, K, Ti, P) and redox-sensitive (Mn, Fe) elements. Inorganic chemistry data provide insights on mineralogy as well as depositional environments and hydrodynamic processes, especially when paired with organic carbon data (Sageman et al., 2003; Algeo and Rowe, 2012; Scott and Lyons, 2012).

Total organic carbon (TOC) was determined using a LECO CS 200 CS-Analyzing System and an UIC Coulometrics Inc. Carbonate Coulometer (Engleman et al., 1985). The LECO method determines total carbon content through combustion of a powdered sample (Jarvie, 1991). Values of TOC were obtained by subtracting total inorganic carbon determined by the coulometer from total carbon. This method is routinely employed in paleoenvironmental analysis due to its accuracy and small sample size requirements (Jackson and Roof, 1992; Schulte et al., 2000; e.g., Böning et al., 2005). The precision of the analysis, based on analysis of internal standards and replicates, was typically better than ± 0.15%. The δ¹³C_org signature of de-carbonated samples was analyzed on a Finnigan MAT Delta plus coupled to a CE elemental analyzer. δ¹³C_org is reported using the delta notation relative to the Vienna Pee Dee Belemnite (VPDB). The uncertainty was less than ± 0.1‰.

Results were analyzed using R software (R Core Team, 2015). Major changes in hydrology and paleoenvironmental conditions were determined using constrained hierarchical cluster analysis of geochemistry and magnetic susceptibility data by the method of incremental sum of squares (CONISS, Grimm, 1987).

Magnetic Susceptibility

Magnetic susceptibility measurements were performed at the Paleomagnetic Laboratory (USPMag) of the Institute of Astronomy, Geophysics and Atmospheric Sciences of the University of São Paulo (IAG/USP). Magnetic susceptibility is used here as a complimentary method to identify significant variations in paleoenvironmental conditions or sediment composition in core XC05. A total of 194 paleomagnetic specimens were collected from the sediment core using cubic plastic boxes (8 cm³) placed side-by-side throughout the core. Low-field magnetic susceptibility of individual specimen was measured using a Kappabridge MFK1-FA system (AGICO Ltd). Two different frequencies (976 and 15616 Hz) were used in a 200 Am⁻¹ field at room temperature (Dearing et al., 1996). All data were mass normalized due to the irregular sample mass inside cubic boxes.

Pollen and Diatom Analyses

Riverbed samples were subsampled for pollen analyses (Table S1). Samples were processed for extraction of pollen grains using the protocol established by Colinvaux et al. (1999). The analyses were performed in the Institute of Geosciences of the University of São Paulo (IGc/USP) under a microscope with magnification of 600x. A minimum of 300 terrestrial pollen grains were counted per sample. Aquatic taxa and spores are not included in the sum of pollen assemblage. The pollen grains and spores were identified using the pollen reference collection of the University of São Paulo and other published reference materials (Erdtman, 1952; Roubik and Moreno, 1991; Colinvaux et al., 1999). The raw pollen count data were entered into the Tilia software (Grimm, 2011), in order to calculate the taxa percentages and concentrations.

Riverbed and sediment core XC05 were subsampled for diatom analyses. Diatom analysis followed standard procedures discussed by Battarbee et al. (2001). Slides were mounted with Naphrax^® as medium. Optical observations and counts were conducted at a magnification of 1000x with a Zeiss Axioskop 2 plus microscope. At least 400 valves were counted per slide. Taxonomy and nomenclature followed published literature sources (e.g., Round et al., 1990; Krammer, 2000; Rumrich et al., 2000; Metzeltin and Lange-Bertalot, 2007) and the on-line catalog of valid names (California Academy of Sciences, 2011).

CH₄ and CO₂ in Sediment Pore Waters

Sediment core XC05 was sub-sampled in field on the same day of collection for the assessment of dissolved methane and carbon dioxide concentrations in pore waters. Aliquots of 5 ml of wet sediment were collected with an open-ended 5 ml polypropylene syringe after carefully drilling holes at 10 cm intervals. Immediately after collection, the aliquots were injected into a 120 ml vial containing 10 ml of NaOH (5%), capped with butyl rubber stoppers and sealed with aluminum crimps. Control standards of ambient air were collected during sampling for corrections. In the Center for Nuclear Energy in Agriculture of the University of São Paulo (CENA/USP), samples were shaken for headspace equilibration and 60 ml of gas sample was retrieved from vials headspace using a 60 ml syringe and analyzed by Cavity Ring Down Spectroscopy using a Picarro G2201-i device. Samples were slowly injected following the pump flow, taking care not to change the internal pressure, which can be monitored by the analyzer. The 60 ml analyzes took approximately 3 min to pass through the analyzer giving a steady measurement for roughly 40 s that was checked with three standard gas mixtures for concentration and carbon isotope composition of CH₄. Reproducibility between replicates presented a variation of the standard deviation >0.5% for concentration and >0.9% for δ¹³C_CH4. Readings of concentration (ppm) and δ¹³C_CH4 (‰) by the analyzer were slightly different than the standard reference values. Thus, sample results were corrected according to a standard calibration curve.

Optically Stimulated Luminescence and Radiocarbon Datings

Optically stimulated luminescence (OSL) dating was carried out in fine silt or sand quartz aliquots from cores XC02, XC03, and XC05 in the Luminescence and Gamma Spectrometry Laboratory of the IGc/USP. Quartz aliquots for luminescence measurements were prepared under subdued red light. Wet sieving and settling procedures were used to isolate the 4–11 or 180–250 μm grain sizes. The target grain size fractions were submitted to oxygen peroxide (H₂O₂) and hydrochloric (HCl 10%) treatments to remove organic matter and carbonates, respectively. Heavy liquid separation of quartz sand grains was performed using lithium metatungstate solution at densities of 2.75 and 2.62 g cm⁻³ to remove heavy minerals and feldspar grains, respectively. Concentrates of quartz sand grains were etched with hydrofluoric acid (HF 38%) for 40 min in order to remove the outer rind of quartz grains damaged by alpha particles and remnant feldspar grains. Luminescence measurements were performed in two automated Risø OSL/TL reader model DA-20 equipped with blue (470 nm) and infrared (870 nm) LEDs for light stimulation, Hoya U-340 filter for light detection in the ultraviolet band and built-in beta radiation sources (⁹⁰Sr/⁹⁰Y) delivering dose rates of 0.088 and 0.135 Gy s⁻¹ (for aluminum discs). Equivalent doses were determined through the single-aliquot regenerative dose protocol (Murray and Wintle, 2000). For fine silt, a mean a-value of 0.04 was considered for calculation of alpha dose rate in quartz. Tests with infrared stimulation indicated absence of feldspar in the fine silt concentrates. A dose recovery test was performed to set up the luminescence measurements protocol to the studied samples batch. Samples equivalent doses were calculated through the Central Age Model (Galbraith et al., 1999). The concentrations of K, ²³⁸U and ²³²Th for dose rate calculations were determined using high resolution gamma spectrometry with a high purity germanium detector (relative efficiency of 55% and energy resolution of 2.1 KeV) encased in an ultralow background shield. Samples were packed in sealed plastic containers and stored for at least 28 days for radon equilibration before gamma spectrometry. Radiation dose rates were calculated using conversion factors outlined by Guérin et al. (2011). Radiation dose rates were corrected for water saturation (water weight/dry sample weight). Cosmic dose rates were calculated through samples latitude, longitude, elevation and burial depth, according to Prescott and Hutton (1994).

Accelerator mass spectrometry (AMS) radiocarbon (¹⁴C) dating was performed on leaves and charcoal fragments retrieved from the sediment cores. Samples were treated in the Radiocarbon Laboratory of the Illinois State Geological Survey and submitted to the Keck Carbon Cycle AMS Laboratory of the University of California-Irvine for AMS ¹⁴C analysis. The ¹⁴C dates were calibrated using the program Calib 7.0 and the calibration curve IntCal 13 (Stuiver and Reimer, 1993; Reimer et al., 2013).

Results

Geochemistry of Suspended and Riverbed Sediments

Geochemical results are summarized in Tables 1, 2 (discretized dataset in Table S1). Strong variations in suspended sediment composition were identified between wet and dry seasons in the Xingu, Tapajós, and Amazon rivers (Table 1, Figure 3). Seasonal changes in suspended sediments of the Xingu and Tapajós rivers include the increase in the relative amount of P in sediments of the dry season, which is directly related to primary productivity (Engstrom and Wright, 1984; Dean and Gorham, 1998). The P/Ti ratio is an effective proxy to evaluate the sedimentation of phosphorous regardless of terrigenous input and it avoids dilution effects caused by changes in sedimentation rate (Latimer and Filippelli, 2002; Filippelli et al., 2003). Average P/Ti ratios in the Xingu River vary from 0.66 in the wet season to 4.20 in the dry season. Seasonal changes in P concentration have lower amplitudes in the Tapajós River, with the P/Ti ratio shifting from 0.75 to 0.94 from the wet to the dry seasons, respectively. The Fe/K ratio is a useful indicator of mineralogical stability, since the most stable rock-forming minerals have lower Fe/K ratios (K-feldspar, muscovite, and quartz) and unstable minerals tend to be richer in iron content (Herron, 1988; Armstrong-Altrin and Machain-Castillo, 2016). Fe/K ratios increase during the wet season both in the Xingu and Tapajós rivers, with relatively little variation in the Amazon River (Table 3). In the Xingu River, Ca concentrations increase from 0.09 to 0.35 mg l⁻¹ and P concentration from 0.03 to 0.71 mg l⁻¹ between the wet and dry season. Fe concentrations shift from 1.11 to 2.56 mg l⁻¹ from the wet to the dry season. The inverse pattern is observed in the Amazon River, with Ca, P, and Fe concentrations decreasing in the dry season (Table 1, Figure 3). In the Tapajós River, these shifts between wet and dry seasons have lower amplitude, with Ca concentration varying from 0.07 to 0.13 mg l⁻¹, P varying from 0.03 to 0.05 mg l⁻¹ and Fe varying from 0.99 to 0.76 mg l⁻¹.

TABLE 1

Table 1. Variation of major elements concentrations in suspended sediments of the Xingu, Tapajós, and Amazon rivers during the wet and dry seasons.

TABLE 2

Table 2. Summary of major elements concentrations, TOC and δ13C_org of bulk organic matter in bottom sediments of the Xingu, Tapajós, and Amazon rivers.

FIGURE 3

Figure 3. Scatterplots comparing P, Ti and K concentrations in suspended sediments collected in the Xingu, Tapajós and Amazon rivers during the wet and dry seasons.

TABLE 3

Table 3. Variation of elemental ratios in suspended sediments of the Xingu, Tapajós, and Amazon rivers during the wet and dry seasons.

Pollen and Diatoms in Riverbed and Core Sediments

In total, 45 pollen taxa were identified in riverbed sediments of the Xingu Ria (Figures S1–S4). The vegetation represented by pollen retrieved from riverbed sediments has great diversity and high percentages of forest elements. Arboreal taxa encountered in the samples include Acalypha, Alchornea, Annacardiaceae, Apocynaceae, Arecaceae, Attalea, Bignoniaceae, Cecropia, Combretum, Dalbergia, Didymopanax, Euterpe, Fabacea, Genipa, Machaerium, Mauritia, Mauritiella, Matayba, Melastomataceae, Mimosa, Myrtaceae, Palmae, Psidium, Psychotria, Sapium, Spondias, Sterculiaceae, Stigmaphyllon, Talisia, and Zygia. Terrestrial herbaceous elements are represented by Alternanthera, Asteraceae, Bambusa, Begonia, Caesaria, Lamiaceae, Phyllanthus, Pilea, Poaceae, Polygonaceae and Symmeria. Sagitaria, Cyperaceae, Alismataceae represent taxa of aquatic herbs. Spores identified in the analysis include Polypodiaceae, trilete and Monolete. The palynologic data indicate that riverbed sediments of the Xingu Ria record the input of sediments from areas where the predominant vegetation type is forest (Figure S5).

Regarding the diatoms, a total of 65 infrageneric taxa were identified in riverbed sediments of the Xingu Ria. Eunotia and Gomphonema were the most represented genera regarding species number (24.6% of total species), followed by genus Aulacoseira (9.2%) (Figure S6). Eunotia species are mostly acidophilic, oligotrophic, and typified by a dominant periphytic habitat (Round et al., 1990; van Dam et al., 1994; Moro and Fürstenberger, 1997; Hamilton and Siver, 2010). Due to the secretion of mucilage by the apical pore fields, Gomphonema is a common genus in periphytic algal communities, being well represented in richness and density (Tremarin et al., 2009). Aulacoseira is a common planktonic genus inhabiting lacustrine and running freshwaters, developing in various trophic conditions (Denys et al., 2003; Zalat and Vildary, 2007). Ecological information at species level is required to use this genus as indicator of water quality (Bicudo et al., 2016).

Diatoms presented well-preserved frustules throughout the core. Assemblages from the core XC05 base showed little variation among genera, and besides the planktonic genus Aulacoseira, comprised benthic and periphytic genera that require surfaces for developing (e.g., Eunotia, Pinnularia and Surirella), suggesting a water column under acidic and oligotrophic conditions with high light penetration. Genera Surirella, Diploneis, Aulacoseira, Placoneis, Gomphonema, Encyonema, and Eunotia were observed throughout the core, suggesting a relatively uniform slack water environment.

Chronology, Magnetic and Geochemistry Data of Sediment Cores

Sediments of the three studied underwater cores (XC02, XC03, and XC05) are composed of dark gray to brown organic-rich muddy sediments. As highlighted in Figure 2, these sediments are similar to the modern surface sediments that accumulate in most of the rias. Samples from the top and bottom of sediment cores XC02 (10–293 cm), XC03 (10–363 cm) and XC05 (45–440 cm) were collected for OSL dating. The luminescence ages of cores XC02, XC03, and XC05 ranged from 118 ± 81 to 4,086 ± 159 years (Table 4), suggesting that the Xingu Ria is a slack water environment acting as trap of fine-grained sediments at least since the middle Holocene. XC02 sediments showed ages from 2,503 ± 462 to 3,295 ± 542 years. XC03 and XC05 sediments cover periods from 118 ± 81 to 1,251 ± 211 years, and from 3,025 ± 185 to 4,086 ± 159 years, respectively. Sediment depth profiles described in the islands of the head of the Xingu Ria (EMB13-07, EMB13-13 and EMB13-17) show dark gray organic-rich sediments interlayered with sands and light gray floodplain sediments (Figure 4). Radiocarbon ages obtained in the dark gray muds, which likely represent buried ria sediments, varied from 141–267 to 5,479–5,580 cal years BP (Table 5, Figure 4).

TABLE 4

Table 4. Radionuclides concentrations, radiation dose rates, equivalent doses and luminescence ages of sediment samples retrieved from cores XC02, XC03, and XC05.

FIGURE 4

Figure 4. Radiocarbon ages in sediment depth profiles of stabilized bar of the Xingu Ria head. Ria sediments are represented by organic-rich muds buried by organic-poor floodplain sediments.

TABLE 5

Table 5. Radiocarbon ages of sediment cores EMB13-07, EMB13-13, EMB13-17, and EMB13-21.

Luminescence and radiocarbon ages allowed the calculation of sedimentation rates for the organic-rich sediments of the Xingu Ria. In the Xingu Ria, sedimentation rates calculated through luminescence ages of core XC05 varied between 0.27 cm yr⁻¹ and 0.70 cm yr⁻¹ (average of 0.37 cm yr⁻¹). The rate of deposition of core XC05 increases from about 0.28 cm yr⁻¹ during the period of ~4,100 to ~3,300 years ago to an average of 0.60 cm yr⁻¹ during the period of ~3,300 to ~3,000 years ago. Cores XC02 and XC03 presented average sedimentation rates of 0.36 cm yr⁻¹ and 0.31 cm yr⁻¹, respectively. Sedimentation rates for organic-rich sediments underneath floodplain sediments of the Xingu Ria head were 0.24 cm yr⁻¹, 0.78 cm yr⁻¹, 0.05 cm yr⁻¹ in profiles EMB13-07, EMB13-13 and EMB13-17, respectively (Figure 4). In the Tapajós Ria, sedimentation rates were calculated through radiocarbon ages presented in Irion et al. (2006). Rates of sediment deposition in the Tapajós Ria vary from 0.24 cm yr⁻¹ to 0.65 cm yr⁻¹ (average of 0.37 cm yr⁻¹).

Magnetic susceptibility measurements were performed on the XC05 core. Low-field magnetic susceptibility varies from 3.4 × 10⁻⁸ to 1.9 × 10⁻⁷ m³kg⁻¹ (Figure 5). Strong magnetic susceptibility variations (peaks) may indicate variations in sedimentation rate or increased magnetic mineral concentrations. The dendogram of geochemical data demonstrates abrupt shifts in the compositional similarity of sediments deposited at 3,690–3,650, 3,345–3,335, and 3,235–3,240 years ago. These shifts fit well with peaks in magnetic susceptibility and P, Fe, Mn, and TIC concentration as well as with the decrease in TOC and lithophilic elements (Figure 5).

FIGURE 5

Figure 5. Variation of magnetic susceptibility (χ), CH₄ concentration, δ¹³C_CH4 and major elements geochemistry in sediment core XC05. Grey areas reveal abrupt shifts in compositional similarity of sediments highlighted by hierarchical cluster analysis.

Ti concentration reveals significant positive correlations with Al (r = 0.81, n = 198) and K (r = 0.75, n = 198). These elements were used as proxies for the relative contribution of terrigenous sediment input from the Xingu River to the downstream Xingu Ria lake (Engstrom and Wright, 1984; Boës et al., 2011). Results show significant inverse correlation among P concentration and lithophilic elements represented by Ti (r = −0.31, n = 198), Al (r = −0.32, n = 198) and K (r = −0.46, n = 198). P concentration also shows significant positive correlations with Fe (r = 0.57, 198), TIC (r = 0.51, n = 198) and Mn (r = 0.51, n = 198).

Total organic carbon (TOC) concentration varies between 1.77 and 3.35% (average of 2.45%) in sediment core XC05. The measured concentrations are similar to values in samples from bottom sediments of the Xingu Ria (Häggi et al., 2016). Values of δ¹³C_org range from −31.04 to −27.49‰, and indicate that organic matter from bottom sediments of the Xingu Ria is mainly derived from arboreal C3 vegetation (Table S1). This is supported by palynological data, with pollen assemblages dominated by forest taxa (Figure S1).

CH₄ concentrations in pore waters reach values up to 25% (volume) in XC05 sediment core (Figure 5). The values of δ¹³C_CH4 in pore waters of XC05 core range from −71 to −57‰ PDB. Higher (more positive) values of δ¹³C_CH4 often agree with peaks in magnetic susceptibility, Fe concentration and P/Ti (Figure 5). This suggests that CH₄ oxidation in pore waters might increase during drier periods.

Discussion

Despite the relatively low suspended load in clearwater rivers, the composition of suspended sediments in the Xingu and Tapajós rivers are organic-rich in comparison with white water rivers, showing a marked variation between the dry and wet seasons. Major variations in sediment composition occur due to seasonal changes of hydrology, driving the input of organic and inorganic compounds and regulating primary productivity. The seasonal changes in river discharge controls the relative concentrations of lithophilic elements (Ti, Al, K) compared to elements influenced by redox conditions in the water column and riverbed (P, Fe, Mn). While the uncertainty of organic carbon sources and its stability through time limits its use as proxy for lake productivity or paleo-redox conditions, phosphorous concentration is a useful indicator of paleo-productivity (Engstrom and Wright, 1984; Dean and Gorham, 1998; Boyle, 2001). In order to compensate for fluctuations in allochthonous (terrigenous) inputs of sediments to the ria lake, the P to Ti ratio was chosen as productivity indicator (Latimer and Filippelli, 2002; Filippelli et al., 2003). Average P/Ti values vary from 4.20 to 0.66 in suspended sediments of the Xingu River during the dry and wet seasons, respectively. The higher values during the dry season are linked to higher primary productivity favored by low water turbidity.

There are significant positive correlations between Fe and Ca (p = 0.71, n = 198), Fe and P (p = 0.57, n = 198) and Fe and TIC (p = 0.97, n = 198) concentrations in core XC05, which point to biogeochemical controls on Fe and TIC deposition in sediments. The high concentration of Fe relative to K in suspended sediments transported during the dry season suggests that assimilation of Fe in sediments is favored by the increase in organic productivity and oxygenated bottom waters (Table 3). Major decreases in TOC concentrations are correlated to peaks of P/Ti, TIC, Fe and Mn, suggesting lower preservation of organic matter during drier periods (Figure 5). The lack of correlation between TOC and TIC in core XC05 indicates that the shallow bathymetry during drier low-water periods likely decreased calcite solubility, enhanced evaporation and led to the elevated concentration of the carbonate ions (Kelts and Talbot, 1990). Mn and Fe in sediments are remobilized under reducing conditions and precipitated in the presence of oxygenated waters (Davison, 1993). Lower values of Fe/Mn ratios, proposed by Mackereth (1966) as a redox proxy, are correlated with peaks of P/Ti, suggesting abrupt shifts in redox conditions during sediment deposition in the Xingu Ria. Peaks of P/Ti indicate dominant wetter conditions punctuated by dry events at 3,690–3,650, 3,345–3,335, and 3,235–3,240 years ago (Figure 5). Nutrient-rich and oxygenated waters favor the accumulation of P, Fe and Mn in sediments deposited under drier and low-water level periods. In contrast, TOC is negatively correlated with P, Fe and Mn concentrations due to the lower organic matter preservation under oxic conditions prevailing during drier periods. During the low water season, the shallower water column would be better mixed and the oxic water in contact with the bottom sediment would lead to a faster degradation of the deposited organic matter. Thus, considering the redox and productivity proxies already described, the variation in TOC concentration through time is mainly derived from changes in the water-sediment interface from anoxic/dysoxic (higher TOC) to oxic (lower TOC) conditions that may be related to hydrologic changes in the area drained by the Xingu River.

Fine-grained sediments accumulated in Amazon rias have relatively high concentration of organic carbon (average TOC of 2.45%) compared to fine-grained sediments deposited in floodplains under influence of white water rivers such as the Amazon River (0.4–1.4%; Moreira-Turcq et al., 2004; Aniceto et al., 2014; Moreira et al., 2014). Thus, rias formed in large clearwater rivers such as the Xingu and Tapajós rivers act as hotspots for carbon storage within rivers in the Amazon Basin. These areas are present at least since the middle Holocene, considering the ages obtained for the sediment cores from the Xingu (>4,000 years, this study) and Tapajós rivers (>9,600 years, Irion et al., 2006). Stable carbon isotope data (δ¹³C_org from −31.04 to −27.49‰) indicate a dominant contribution of C3 plants and possibly phytoplankton for the organic particles accumulated in the ria bottom. Palynological data document a large contribution of C3 arboreal plants as major sources of carbon in sediments of the Xingu and Tapajós rias. The labile organic matter derived from phytoplankton may be rapidly consumed and turned into CO₂ in the oxic surface sediment layer, while the more recalcitrant terrestrial organic matter accumulates. Also, once buried in the anoxic sediment, the autochthonous and labile organic matter may be used to fuel the CH₄ production within sediments. This mechanism is in accord with the high CH₄ concentrations in pore waters and released to the atmosphere obtained by this work and by Sawakuchi et al. (2014). Despite the large carbon storage, the Xingu and Tapajós rias show the highest fluxes of CH₄ to the atmosphere among the major Amazon tributaries (Sawakuchi et al., 2014), suggesting that sedimentary conditions suitable for organic matter preservation favor anoxic conditions in the sediments, where CH₄ can be produced and released to the atmosphere. This is supported by the high concentrations (up to 24%) of CH₄ in sediment pore waters of the Xingu Ria, with δ¹³C_CH4 varying from −70.4 to −56.9‰, suggesting low CH₄ oxidation rates. These results indicate that rias in clearwater Amazon rivers are significant organic carbon sinks and sources of CH₄ to the atmosphere. They should be considered as distinct environments in the Amazon in order to refine modern carbon balance assessments.

The pollen assemblages show a high diversity of arboreal taxa, pointing to the terra firme and igapó forests as main sources of organic matter within sediments of the Xingu River catchment. Despite the increasing deforestation in the Xingu catchment during the last several decades (Barona et al., 2010), organic carbon stored in riverbed sediments is mainly derived from forest. This could be related to a delay in transfer of the deforestation signal to river sediments, or a dominant input of organic matter from the igapó flooding forest tract along the river channel. The diatom assemblages in riverbed sediments and the sediment core point to a slack water environment in the Xingu Ria since the middle Holocene. Considering that the organic matter pool in sediments of the Xingu and Tapajós rias is mainly terrigenous and derived from forested areas, the input of carbon to the ria sediments is favored during high precipitation episodes while carbon preservation is controlled by duration and frequency of dry periods. Low sedimentation rates combined with well oxygenated waters due to higher primary productivity in the water column favor organic matter degradation in riverbed sediments during dry periods. Despite high rates of organic matter degradation during low-water periods, the higher primary productivity favors the uptake of CO₂ and carbon recycling in the water column and riverbed. During high-water phases, the flux of CO₂ to the atmosphere increases due to lower primary productivity, while higher sedimentation rates favor organic matter preservation and carbon uptake in sediments. High primary production is the main indicator of CO₂ undersaturation observed in large clearwater rivers in the Amazon during the low-water phase (Rasera et al., 2013).

The sediment cores retrieved in the Xingu Ria have ages varying from 3,025 ± 185 to 4,086 ± 159 years (XC05), from 118 ± 81 to 1,251 ± 211 years (XC03) and from 2,503 ± 462 to 3,295 ± 542 years (XC02). The cores were collected in the deepest part of the river profile and core tops with ages between 3,025 ± 185 (XC05) and 2,503 ± 462 (XC02) years indicate erosional processes and sediment reworking within the ria. The lack of recent deposits indicates that erosion due to channel migration may remobilize sediments in certain portions of the ria. The average sedimentation rate obtained in this study for the Xingu Ria is 0.35 cm yr⁻¹ since the middle Holocene (~4,000 years). On millennial timescales, sediment deposition rates at different locations are relatively stable. A similar average sedimentation rate of 0.37 cm yr⁻¹ was also observed for the Tapajós Ria over the last ~11,000 years Irion et al. (2006). Sedimentation rates from 0.35 to 0.37 cm yr⁻¹ are relatively high compared to sedimentation rates observed in low latitude lakes, which are typically around 0.05 to 0.25 cm yr⁻¹ (Cross et al., 2000; Chu et al., 2002; Hodell et al., 2005; Caballero et al., 2006; Conroy et al., 2008; McGlue et al., 2011). Our data show that sedimentation rates varied through time in core XC05. The temporal and spatial variations in sedimentation rates would result from hydrologic changes and sediment reworking within the Ria. The migration of underwater channels and wave action would be the major autogenic processes responsible for sediment remobilization and spatial changes in sedimentation rates. Temporal variations would also be related to precipitation changes affecting sediment supply and accommodation space within the ria. Additional data are required to calculate sedimentation rates with higher temporal resolution and allow a comparison with paleoprecipitation records. This is necessary to constrain the major controls on sedimentation rates and the role of precipitation changes for carbon burial. The TOC concentration in core XC05 varies from 1.77 to 3.35% (average of 2.45%), similar to TOC values measured in bottom sediments collected in the Xingu Ria (average of 2.36%) (Häggi et al., 2016). Irion et al. (2006) showed TOC values with low variation in the Tapajós Ria, varying from 2.2 to 2.9% in sediments younger than 7,500 years. The high sedimentation rates would reduce the effectiveness of degradation processes, implying that the Xingu and Tapajós rias are potentially massive carbon sinks on a millennial timescale.

We estimated rates of organic carbon burial in the Xingu and Tapajós rias based on a dry bulk density of 1.3 g cm⁻³ for the bottom ria sediments, average sedimentation rates of 0.35 cm yr⁻¹ and 0.37 cm yr⁻¹ (Irion et al., 2006) for the Xingu and Tapajós rias, respectively, and the minimum and maximum TOC concentrations obtained in this work and by Irion et al. (2006). In the Xingu Ria, carbon burial ranges from 84 g m⁻² yr⁻¹ to 159 g m⁻² yr⁻¹ (average of 116 g m⁻² yr⁻¹) and from 106 to 169 g m⁻² yr⁻¹ (average of 121 g m⁻² y⁻¹) in the Tapajós Ria. Assuming that 75% (conservative estimate) of the ria surface is covered by fine-grained organic-rich sediments (Figure 2), the Xingu Ria buries from 0.08 Tg C yr⁻¹ to 0.16 Tg C yr⁻¹ (average of 0.11 Tg C yr⁻¹) and the Tapajós Ria buries from 0.19 Tg C yr⁻¹ to 0.30 Tg C yr⁻¹ (average of 0.21 Tg C yr⁻¹). Conceding that the Xingu and Tapajós Rias were totally flooded at least since the middle Holocene (~5,000 years), around 560 Tg C and 1050 Tg C of carbon are stored in sediments of the Xingu and Tapajós rias, respectively.

A rough attempt to estimate the carbon budget of the Xingu Ria is possible considering the average accumulation rate of carbon in sediments of the Xingu Ria of 0.11 Tg C yr⁻¹ (this study) and the carbon evasion estimates of 8 Tg C yr⁻¹ as CO₂ (Sawakuchi et al., this volume) and 0.053 Tg C yr⁻¹ as CH₄ (Sawakuchi et al., 2014) fluxes to the atmosphere. These estimates indicate that despite the significant carbon pool and storage, the Xingu Ria is a net source of carbon to the atmosphere. Furthermore, the Xingu Ria can serve as an analog for sediment accumulation and carbon processing in the reservoirs of the Belo Monte hydropower plant. The multidecadal carbon sedimentation pattern estimated for the Xingu Ria allows projections about sediment accumulation and carbon processing in the Belo Monte reservoirs.

Conclusions

The lowermost sectors of the Tapajós and Xingu rivers have lake-like (fluvial ria) sedimentary dynamics due to the impoundment by the Amazon mainstream during the Holocene. This lake-like physiography hinders the transfer of sediments to the Amazon River and induces the accumulation of fine-grained organic-rich sediments derived from upstream areas. Thus, the downstream reaches of these major clearwater rivers are sinks for particulate organic matter chiefly derived from arboreal forest (terra firme and igapó). Wetter periods favor the supply and preservation of forest-derived organic matter in sediments while drier periods increase the organic productivity in the water column and favor degradation of organic matter in riverbed sediments. Microbial consumption of organic matter in the oxic surface layers of the sediment contributes to the anoxic conditions that prevail within sediments, with methanogenesis being an important path for biodegradation of particulate organic matter. During dry and low-water level periods, the flux of CH₄ to the atmosphere increases while the CO₂ flux decreases due to the higher organic productivity within the water column. Thus, seasonal variations play an important role for carbon dynamics in clearwater rivers. Despite the significant carbon storage that occurs in the Xingu and Tapajós rias at least since the middle Holocene, our carbon balance estimates indicate that Amazon rias would act as source of carbon to the atmosphere. A future drier climate as projected for eastern Amazonia would reduce the carbon sink potential of clearwater rivers and increase the methane flux to the atmosphere.

Author Contributions

DJB, AS, and HS were responsible for design of the study and preparation of the manuscript. AS, HS, GH, DJB, and FP organized overall project logistics. DJB and HS executed the sampling and analysis of CH₄ in sediment core and performed calculations of carbon balance. FP and AS executed luminescence dating. GH performed magnetic susceptibility analysis. MM, FP, and DJB performed sampling and geochemical analysis of the sediment core. CC, MZ, and ES executed geochemical analysis of suspended and riverbed sediments. TP collaborated with sediment and greenhouse gas sampling and supported local logistics. RS and PO executed palynology analysis. SF and DCB performed diatom analysis. All authors contributed to data interpretation and critically revised the manuscript for final submission.

Funding

This study was funded by FAPESP grants #2011/06609-1, #2014/23334-4, #2016/02656-1 and CAPES grant #AUXPE 2043/2014.

Conflict of Interest Statement

The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

Acknowledgments

We thank Luciana Nogueira and Thays Desiree Mineli for the support with luminescence dating procedures. Bailee Hodelka, Joseph Lucas, and Jason Backus assisted with XRF and coulometry measurements. We also thank the reviewers for constructive criticisms and valuable comments. Open access publication fees were supported by the Gordon and Betty Moore Foundation Marine Microbial Initiative.

Supplementary Material

The Supplementary Material for this article can be found online at: https://www.frontiersin.org/article/10.3389/fmars.2017.00044/full#supplementary-material

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