Abstract
Objective
We described source and phosphorus (P) retention potential of soft, fine-grained, streambed sediment and associated phosphorus (sed-P) during summer low-flow conditions. Combining in-channel, sed-P storage with relative age provided context on relevance to western Lake Erie Basin management goals.
Methods
In 2019, rapid geomorphic assessment (30 reaches) compared streambed-sediment storage (S) to streambank erosion (E), providing annual sediment budgets (S:E). Streambed sediment (13 reaches) was fingerprinted and analyzed for sed-P. The P saturation ratio (PSR; four reaches) quantified potential sorption/desorption of dissolved P (DP) between the water column and streambed sediment. Analyses were supplemented with data from 2017 and 2021. The ratio of two fallout radionuclides, beryllium-7 (54-day half-life) and excess lead-210 (22.3 years), apportioned “new” sediment based on time since rainfall contact.
Results
Streambed sediment was mostly streambank (54–96%) for contributing areas > 2.7 km2; for upstream reaches, a larger percentage was apportioned as upland (cropland, pasture, forest, and road), with < 30% streambank. Streambank erosion correlated with contributing area; however, soil type (ecoregion), stream characteristics, and land use combined to drive streambed-sediment storage. Individual-reach S:E (accumulation of 0.01–35 years of streambank erosion) differentiated erosional and depositional in-channel environments. Most reaches indicated that 17–57% of sediment had recent contact with rainfall. Streambed-sediment PSR indicated a low potential for further sorption of DP from the water column; one reach was a P source when sampled.
Conclusion
Sed-P was higher in streambed sediment than in source samples, which varied by land use and ecoregion. This indicates homogenization resulting from in-stream sorption of DP during sediment transport that occurs over multiple events.
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1 Introduction
Sediment fingerprinting uses a range of physical and biogeochemical properties to differentiate sediment sources (Guzmán et al. 2013; Collins et al. 2020), including an accuracy assessment based on identification of the original source samples (Gellis and Walling 2013). Sediment fingerprinting has been used in basins of 10–100 km2 to apportion streambed-sediment (Williamson et al. 2014; Blount et al. 2022) as well as suspended sediment at event (Cashman et al. 2018), monthly (Fitzpatrick et al. 2019), and seasonal (Boudreault et al. 2019) timescales. Common upland sources of stream sediment include material directly transported from cropland, pasture, and forested parcels as well as that washed from roads that connect the agricultural landscape. Studies in agricultural basins have shown that sediment also commonly includes streambank-derived material, with source contributions varying as a function of physiography, season, and contributing area (Gellis and Noe 2013; Gellis et al. 2014, 2019; Gellis and Gorman Sanisaca 2018; Fitzpatrick et al. 2019; Williamson et al. 2020a).
Measuring streambank erosion in basins where it has been identified by sediment fingerprinting is the next step in guiding resource-management decisions. Geomorphic assessment of the riparian corridor, including both quantification and location of streambank erosion and streambed-sediment storage (Fitzpatrick et al. 2016; Blount et al. 2022), is key to differentiating reaches that provide sediment for transport downstream from those where material accumulates in the channel (Kwan and Swanson 2014; Lamba et al. 2015b; Fitzpatrick et al. 2019; Schilling et al. 2022); together, these provide a sediment budget. Integrating sediment fingerprinting with a sediment budget and fallout radionuclide (FRN)-based chronometers of suspended (Lamba et al. 2015a), streambed (Matisoff et al. 2005), and in-channel exposed (Karwan et al. 2018) sediment provides multiple lines of evidence to guide resource management (Collins et al. 2020).
In the Great Lakes basin, non-cropland land commonly coincides with areas susceptible to erosion, with discontinuous forest marking the irregular valley development at the transition from glacial till to lake-plain sediment (Williamson et al. 2020a; Blount et al. 2022). This glacial till is more erodible than lake-plain sediment (NRCS 2020), resulting in more animal operations along headwater reaches relative to higher-order streams, where cropland is a larger percentage of land use (Homer et al. 2020). Compaction of soil from livestock in pastured uplands reduces plant cover and soil macropore space, causing increased runoff and soil erosion (Foote et al. 2015). Livestock grazing in riparian areas increases streambank erosion (Tufekcioglu et al. 2012), and unmanaged manure is an exposed source of P (Stackpoole et al. 2019).
Fertilizer and manure applications result in dissolved (DP) and particulate P (PP) entering the stream system (Sharpley et al. 1992; Han et al. 2012), with higher potential where soil is easily erodible and when fields are left bare in the early winter and spring (Capel et al. 2018a, b). As P leaves the uplands and is transported through the stream network, it spirals between DP and PP through biotic assimilation and mineralization (Newbold et al. 1983) and is sorbed to(from) suspended and streambed sediment that progressively moves downstream during multiple events (Verhoff et al. 1979). Fine-grained, streambed sediment in agricultural landscapes is commonly saturated with P, increasing the potential for desorption to the water column (Haggard et al. 2007; Palmer-Felgate et al. 2009; Osmond et al. 2012; Kreiling et al. 2019), with in-channel stores of sed-P providing a legacy source on a scale of years to decades (Casillas-Ituarte et al. 2020; King et al. 2021; Williamson et al. 2021a). The proportion of agricultural land use, DP concentrations, and sediment physicochemical characteristics each influence how P is stored or released by streambed sediment (Kreiling et al. 2023). Streambank erosion has been identified as an additional source of sed-P (Collins et al. 2010; Gellis and Noe 2013; Huisman et al. 2013), with concentrations similar to agricultural land (Huisman et al. 2013; Williamson et al. 2014, 2020a; Fitzpatrick et al. 2019), although the cause of these high concentrations may vary among basins.
In recent years, the Maumee River Basin (“the Maumee”; 17,052 km2) was the largest contributor of total phosphorus (TP) to Lake Erie, mostly as non-point sources (Han et al. 2012), despite on-field implementation of conservation management to reduce nutrient runoff related to harmful algal blooms (HABs) and hypoxia in the western Lake Erie Basin (WLEB) (USDA-NRCS 2017; Kast et al. 2021). In recent years, TP in the Maumee has been approximately 20% DP and 80% PP (2009–2013; Scavia et al. 2017). Exchange between DP and PP varies as a function of stream size, substrate, and climatic variability, with DP accounting for 8–42% of TP among tributaries (2015–2018; Williamson et al. 2021b), highlighting that this DP/PP ratio is not static in either space or time. Consequently, management success of upland P is difficult to quantify without understanding riparian-corridor sources and stores, including abundance, transformations, and retention in the stream network. This is also key to prioritizing future conservation management (e.g., Stackpoole et al. 2019; Moriasi et al. 2020).
As part of the Great Lakes Restoration Initiative, long-term continuous monitoring was implemented on Black Creek, Indiana (Fig. 1), an agricultural basin with a mix of cropland, active horse pastures that enable farming and transportation for the Amish community, and rural neighborhoods. This 12-digit hydrologic unit code (041000050104) basin was identified as a significant contributor to nutrient, and sediment loads for the WLEB (Robertson and Saad 2011) and individual reaches, most of which were in western tributaries, were identified as impaired for nutrients, biological communities, Escherichia coli, and streambank erosion (SNRT Inc. 2015). Sediment fingerprinting of streambed (August 23–24, 2017) and monthly suspended-sediment composites during the 2018 water year (October 2017–September 2018) indicated that streambank contributions exceeded those from the combination of upland sources (Williamson et al. 2020a, 2021a). Identification of streambank as a primary contributor shifted the conversation about management and conservation in the basin, and raised questions of why/where erosion was occurring and if streambank stabilization should be considered. To answer this question, our objectives were to
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Fingerprint streambed sediment for apportionment as upland sources and streambank
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Use rapid geomorphic assessment of environmental setting, to quantify
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Streambank erosion occurrence and
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Soft, streambed-sediment storage volumes
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Estimate recency of streambed-sediment accumulation using FRN
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Quantify phosphorus retention in streambed sediment
Each of these was evaluated at multiple reaches within the stream network, with contributing areas of 0.1–32 km2, and aggregated for the most downstream reach. We hypothesized that the relation between streambank erosion and streambed-sediment storage would primarily reflect stream size and would vary as a function of adjacent land use and glacial landform setting for similar-sized streams.
2 Materials and methods
2.1 Study site
The U.S. Geological Survey (USGS) streamflow and water-quality monitoring site at Black Creek near Harlan, Indiana (Site ID 04183038; USGS 2023) is discussed here as BC1. Elevation in the basin ranges from 216 to 261 m above mean sea level (amsl), with stream slopes of 0–5%. Harlan (near BC8, 13, and 22 in Fig. 1) is located near the western boundary of the basin on the Ancient Lake Maumee shoreline (Fisher et al. 2015; approximately 235 m amsl) which marks the transition between the Eastern Corn Belt Plain moraines made of glacial till and the Huron/Lake Erie Plains (Fig. 1; Omernik and Griffith 2014). This boundary is commonly marked by forest in what is otherwise an agricultural landscape. Subsurface drainage is common on lake-plain agricultural fields, with less on glacial till (U.S. Department of Agriculture-Natural Resources Conservation Servise [USDA-NRCS] 2016). Glacial till has high runoff risk and is highly erodible (SNRT Inc. 2015; Porter et al. 2018); active horse pastures are common on till. Additional details on basin physiography are summarized by Williamson et al. (2021a).
Mean precipitation is 1014 mm, mostly as rain, with more than half of the precipitation occurring in spring and summer (NOAA 2023). Below-zero soil temperatures (0–2 cm; USGS Site ID 411229084541103) occur between December and March (22–62 d yr−1; 2015–2020) (USGS 2023). Most of the field descriptions and sampling discussed here were done in 2019 (1045 mm), a wet fall and spring when frequent precipitation resulted in fallow of approximately 30% of local agricultural land.
2.2 Sediment sources
Samples were fingerprinted using the same source samples as a previous analysis of Black Creek suspended and streambed sediment (Williamson et al. 2020a; methods and data in Williamson et al. 2020b). Source samples were collected upstream of BC1 between July and September 2017; as a result, source samples for upstream rapid geomorphic assessment (RGA) sites included those from outside of their contributing area. For upland sources, the top 1–2 cm of soil material was composited along a total transect of 250 m (150 m for roads), with one sample collected every 10 m. Sampled cropland included corn, soybean, wheat, and alfalfa fields under conventional and conservation tillage, with a mix of fertilizer and manure nutrient sources. Sampled pastures were limited to those supporting horses; other animals are generally not pastured in this basin. Forests were unmanaged patches, generally smaller than 0.5 km2, and usually included stream channel. Roads were used as a surrogate for development (impervious surface, buildings, etc. in Homer et al. 2020) and included those among agricultural fields and those in neighborhoods; most were paved. Low and middle streambanks were sampled from exposed soil at 10-m intervals along both sides of a stream for a 150-m reach; locations sampled in 2017 were described as part of the RGA. Only the fine-grained (< 63 μm) fraction was analyzed.
2.3 Rapid geomorphic assessment, streambed-sediment storage, and streambank erosion
A combination of stream corridor land-use distribution, valley type, channel slope, stream order (Strahler 1957), and ecoregion (Omernik and Griffith 2014) was used to select 30 RGA reaches using methods of Fitzpatrick et al. (2016); one reach for ~ 3 km of stream length. Roadside ditches were categorized for the land use that ran along the other side of the road. Reaches were categorized as forest if there was forest upstream of the reach and trees separated the stream from agricultural or developed land on both sides. Most reaches included discharge points (pipes) for subsurface agricultural drainage that extended from the streambanks, regardless of adjacent land use and including forested streambanks.
During July 22–25, 2019 (streamflow at BC1 was 0.038–0.048 m3 s−1), the thickness and spatial extent of soft, mobile, fine-grained (mainly silt and clay) streambed sediment was inventoried along 150-m transects (data and methods in Blount et al. 2021). Streambank erosion was also inventoried (USDA-NRCS Wisconsin 2015); erosion along a shallow waterway in a horse enclosure (BC27) was estimated from an upstream reach (BC26). The ratio of streambed-sediment storage to streambank erosion (S:E; after Fitzpatrick et al. 2019) differentiated erosional (S:E < 1) and depositional (S:E > 1) environments; S:E is discussed in years: Mg km−1/Mg km−1 yr−1. Reach-based descriptions of streambank erosion and streambed-sediment storage and sed-P were extrapolated to the remaining network, including both ephemeral and perennial reaches (Fig. 1) (USGS 2020; Blount et al. 2021).
A subset of 13 RGAs that spanned the range of land use, ecoregion, and stream characteristics were selected for streambed-sediment sampling and FRN analysis and sediment fingerprinting. Soft, mobile, fine-grained, streambed-sediment deposits were sampled with plastic tools during summer low-flow conditions, when the potential for sorption/desorption of P is higher due to the longer contact time of water with the sediment (Withers and Jarvie 2008).
2.4 Fingerprinting of fine-grained sediment
Fingerprinting was focused on the fine-grained (< 63 μm) portion of sediment because this is the fraction most likely to be eroded and transported from uplands as well as (re)suspended by streamflow (Lowrance et al. 2006); metals, including P, are concentrated in finer particles (Sharpley et al. 1992). Indicators included 42 metals as well as C and N forms (SI1); only the fine-grained portion was analyzed. Streambed samples from 2019 (data and methods provided in Williamson and Hoefling 2023) underwent the same analyses as those from the earlier study with the exception that C and N were run at the U.S. Geological Survey Upper Midwest Environmental Sciences Center (UMESC) on a Variomax CN analyzer (Bremner and Tabatabai 1971).
Statistical methods (Gorman Sanisaca et al. 2017) were the same as those from the 2018 study (Williamson et al. 2020a) and account for differences in particle size distribution (median particle diameter [d50]) and reactivity (surface area and organic carbon [OrgC] concentrations) between sources and stream sediment. Chemical and physical data for source samples were used to apportion streambed-sediment samples as a combination of upland sources and streambank. One source sample (321848_c; Williamson et al. 2020b) was removed as an outlier for all samples, reducing the number of source samples to 70: 13 cropland, 14 pasture, 15 forest, 13 road, and 15 streambank samples. Streambed collected in August 2017 (0.018 m3 s−1) was compared to that from 2019 (BC1,7,8; Williamson et al. 2020c).
Source apportionment and an accompanying source verification were run individually for each target with a 1000-iteration Monte Carlo analysis; allocations of less than 0.5% were considered zero. Mean values from the 1000 iterations are reported here. Source-verification goodness of fit ranged from 72 to 92%, with the exception of one sample (BC22; 61%). Overall, 18 of 70 individual source samples were mis-classified for 1–11 targets; no forest samples were mis-classified, and nothing was mis-classified as road (SI2).
2.5 Proportion of new sediment in bulk streambed using fallout radionuclides
Beryllium-7 (7Be) and lead-210 (210Pbxs) are primarily delivered during rain events to exposed surface soil or sediment. Their different half-lives (7Be 53.3 days, 210Pb 22.3 years) provide a mechanism to differentiate material that has moved within weeks to months versus that moving on the order of decades (Matisoff et al. 2005). Excess 210Pb (210Pbxs) accounts for the 210Pb that exceeds that from Radium-226 (226Ra) decay and is attributed to atmospheric deposition of the 210Pb decay product of Radon-222, which diffuses from the subsurface to the atmosphere.
Unsieved, bulk streambed from 12 RGA reaches (omitted BC10) was analyzed at the University of Minnesota (UMN) FRN laboratory according to standard gamma counting methods (Karwan et al. 2016; method details and data available as Karwan and Williamson 2023). 210Pbxs was computed as the difference of total 210Pb and supported 210Pb based on the daughters of 226Ra–214Pb and Bismuth-214 (Mabit et al. 2014). Contact with metal was avoided so that the same samples could later be sieved and analyzed for trace elements for sediment fingerprinting. Streambed 7Be/210Pbxs was evaluated as the fraction of new sediment after Matisoff et al. (2005):
A precipitation ratio (denominator) of 4 was based upon regionally (Minnesota and Wisconsin) collected, summer precipitation from 2019 (Hankins 2023). While the 7Be signature can vary among and within individual events, this 7Be/210Pbxs ratio varies less (Matisoff et al. 2005), enabling relative comparison of sediment among sites that may reflect accumulation of days to years. This method quantifies “time since rainfall contact”; the ratio translates to a site-specific proportion of sediment recently in contact with precipitation (Matisoff et al. 2005). Based on the range of 7Be activity in these streambed samples, 7Be would remain detectable for between 5 months (median) and 1 year (maximum value) after collection. Hence, we assign the timeframe of months using this method with our data.
2.6 Phosphorus retention potential of bulk sediment
Additional streambed sediment was collected July 8, 2019 (0.076 m3 s−1) and July 13, 2021 (1.10 m3 s−1 up from 0.10 m3 s−1 the previous day) at four RGA sites (BC1, 7, 8, 18) to characterize the potential to retain P (Kreiling et al. 2022). Unsieved, bulk samples were analyzed at UMESC for equilibrium P concentration (EPC0; Kreiling et al. 2019; Kreiling et al. 2023), total elemental P concentration (sed-PBulk; USEPA 1996), particle size distribution (Durner et al. 2017), and d50Bulk. Water samples were also collected at each site and analyzed for DP (Standard Methods 2021). The EPC0 is the concentration of DP in the water column where there is no net sorption or desorption of P to the sediment and can be considered an index of the sediment P-buffering capacity (Simpson et al. 2021), with finer material generally having a higher buffering capacity (Sharpley et al. 1992). Streambed sed-PBulk provided a complement to sed-P of the fine-grained, RGA streambed sediment. Bulk streambed sediment collected in 2019 was analyzed for Mehlich-3 (Meh) P, aluminum (AlMeh), and iron (FeMeh) concentrations at the UMN Research Analytical Laboratory (Mehlich 1984); these were compared to values for bulk source samples and streambed sediment sampled as part of sediment fingerprinting in 2017 (data and methods in Perner et al. 2022). The P saturation ratio (PSR) of sediment, another index of the sediment P-retention potential, was calculated using molar concentrations of the PMeh, AlMeh, and FeMeh. The potential for the streambed sediment to adsorb additional P is indicated by PSR < 0.10; PSR > 0.15 indicates a potential for the sediment to be a source of P to the water column (Nair 2014).
2.7 Statistical methods
Statistical analyses were done in R (R Core Team 2022). Spearman rank-based correlations were used to compare watershed attributes to streambank erosion, streambed-sediment storage, apportionment of streambed sediment, and proportion of new sediment as well as influence of land use and ecoregion. Tukey box plots were used to compare the sed-P and sed-PMeh among sources and streambed sediment; these populations were also evaluated using pairwise Wilcoxon rank-sum tests (Benjamini and Hochberg 1995). Statements of significance indicate a p value ≤ 0.05. Letters included on graphs indicate significantly different groups: a differs from b but ab cannot be differentiated from either.
3 Results
3.1 Land use as a function of ecoregion
Land use was similar among the 30 described RGA reaches and the 13 reaches for which streambed sediment was fingerprinted (Fig. 1, Table 1). Land use differed between glacial till and lake plain, with more pasture upstream of glacial-till reaches (p value = 0.0033) and more cropland upstream of lake-plain reaches (p value = 0.0294). More developed area was upstream of lake-plain reaches (p value < 0.0001), highlighting the density of roads in the rural community centered on the ancient shoreline. In contrast, forest was similarly distributed in both ecoregions (7% median area), mostly in the riparian corridor or near the ancient shoreline.
3.2 Source apportionment of streamed sediment
Apportionment of streambed sediment as cropland was consistently less than the percentage of the contributing area (Fig. 1, Table 1, SI3a). In contrast, pasture apportionment exceeded land use percentage at three reaches (BC18, 25, 26; SI3b), and road apportionment exceeded developed area at two sites (BC22, 25; SI3d). Road-sediment apportionment correlated to developed area (rho = 0.66, p value = 0.0160). Reaches near or downstream of the transition from till to lake plain generally had a forest apportionment that exceeded the land-use percentage (SI3c).
Apportionment of streambed sediment as streambank increased as contributing area increased (SI3e), with contributing areas > 2.7 km2 having 55–96% streambank, regardless of ecoregion. The small lake-plain site below this threshold (BC22) exceeded the streambank apportionment for small glacial-till sites (BC18, 25, 26). More sediment was apportioned as streambank in 2017 than in 2019 for the two lake-plain sites (BC1, 8), with ≥ 55% streambank in each year (Fig. 1).
3.3 Streambank erosion and streambed-sediment storage
Evidence of streambank erosion from field measurements along RGA reaches increased with increasing contributing area and stream order (Fig. 2a, b), with a general inverse correlation with stream slope (Fig. 2c) but no correlation to streambed-sediment apportionment as streambank. Soft, streambed-sediment storage had a general inverse correlation to stream order (Fig. 2e), with highest storage where slope was < 1% (Fig. 2f). Stream slope inversely correlated to drainage area (Fig. 2g; rho = − 0.37, p value = 0.0226). Fluvial erosion of streambanks was the predominant mechanism, but slumping of valley sides or terraces into the channel was observed at the two sites with the highest erosion (Figs. 1 and 2; BC1, 21).
The transition from second- to third-order tributaries generally coincided with the shoreline feature separating glacial till from lake plain (Figs. 1 and 2b, e). Streambank erosion (Figs. 2 and 3) was higher downstream of this feature (p value = 0.0468), which was commonly marked by forested patches (Figs. 1 and 2b). Median streambank erosion along forest reaches (92.6 Mg km−1 yr−1) exceeded that for cropland and pasture reaches (4.4 and 1.5 Mg km−1 yr−1; p value ≤ 0.0151). Soft, streambed-sediment storage was highest along reaches with < 0.7 km2 contributing area (Fig. 2d; p value < 0.0001) but did not vary by land use.
3.4 Streambed-sediment characteristics and comparison to source samples
The fine-grained portion of streambed-sediment and source samples was compared to determine how sediment varied as a function of transport from source environments and through the stream network. Streambed-sediment d50 (3–20 μm) was coarser (p value = 0.0002) than source samples (1–26 μm). Sed-P in streambed-sediment (870–1520 mg P kg−1) exceeded that of most sources (134–1670 mg P kg−1), with the exception of pasture samples (Fig. 4a). Streambed-sediment d50 differed as a function of ecoregion (p value = 0.0391), not land use, reflecting the steeper stream slope (p value < 0.0001) on glacial till (median = 0.84%) relative to lake plain (0.54%). Streambed-sediment d50 from glacial-till reaches, mostly first- and second-order streams, was finer (6.6–11.5 μm) than that from lake plain reaches (3.0–20.1 μm), mostly third- or fourth-order streams. This particle-size difference did not translate to a difference in streambed-sediment sed-P, nor was sed-P distinguishable by land use at individual reaches. For comparison, sed-P in non-road source samples was lower for lake-plain relative to glacial till (p value = 0.0210; median 905 versus 1030 ppm) although d50 was not differentiable (p value = 0.2148). When road samples were included, sed-P was not differentiable between ecoregions (p value = 0.2095).
Extractable elements were measured in bulk samples for both sediment and source samples. Pasture PMeh was higher than other source samples and streambed sediment (Fig. 4b), with higher sed-P in fines (Fig. 4a inset) that was most similar to streambank samples. Pasture samples were more saturated than other sources and indicated potential release of P to the dissolved phase, with PSR above the 0.15 threshold (Fig. 4c). In contrast, road samples had lower P relative to other sources, with high PSR that reflected low FeMeh + AlMeh availability (< 11 mmol compared to 5–48 mmol among other land use types). Most cropland and forest samples showed potential to sorb additional P. Median streambank-sample PSR was in the transition between the potential to adsorb and the potential to release P.
Comparison of sed-P with d50 for bulk and fine-grained streambed sediment underscores the higher concentrations in finer material (Fig. 4a and Table 2). All years had similar PMeh (Fig. 4b; median = 41 ppm), accounting for 5–15% of total sed-P for streambed sediment (2019 and 2021). Based on PSR for bulk sediment, streambed at these four sites was at or close to being saturated with P (Table 2 and Fig. 4c). In 2019, when streamflow was the highest of the years sampled, the three larger sites indicated potential release of P from streambed sediment to the water column. PSR from 2021 and 2017 showed only one of three sites above the threshold, with ranges that were similar to streambank source samples. At three of the four sites, EPC0 values were less than the measured water column DP (Table 2), indicating streambed sediment as a potential P sink when sampled. Only BC7 was a potential P source and only in 2019.
3.5 Differentiating erosional and depositional environments in stream network
3.5.1 Bed-sediment accumulation as a function of streambank erosion
There was no consistent relation between RGA reach-specific streambank erosion and streambed-sediment storage (Fig. 3, SI4). Median streambed-sediment storage was 6 Mg km−1 (mean = 29 Mg km−1). Median streambank erosion was 10 Mg km−1 yr−1 (39 Mg km−1 yr−1). Two described reaches had no measurable bed sediment, four reaches were stabilized as grassed waterways, and two were grassed, roadside ditches. Some grassed waterways and roadside ditches had enough channelized flow to result in active streambank erosion, and one pasture site had a poorly defined channel that precluded estimation of streambank erosion. For three reaches, the S:E was 0.01–0.03 yr (Fig. 3 circles), indicating an erosional environment where material is transported out of the reach and downstream on the order of days. Five additional reaches had an S:E < 0.3 yr, indicating an erosional environment but with seasonal accumulation of sediment. Four reaches indicated a depositional environment and storage of sediment from upstream sources, with years (S:E = 3–5 yr) to decades (S:E = 12–35 yr) of material stored in the stream channel. One pasture reach had evidence of long-term sediment storage (S:E > 100 yr). Mean S:E (14 yr) exceeded median S:E (0.2 yr) by two orders of magnitude; storage and erosion showed similar patterns.
Cumulative streambank erosion and streambed-sediment storage upstream of each RGA reach give an indication of the overall variability in erosion and storage and how it potentially changes through the basin (SI5). At BC1, the most downstream reach, this totaled 1300 Mg km−1 yr−1 and 2200 Mg km−1, respectively, indicating 1–2 yr worth of upstream streambank erosion accumulated in the upstream network. Twelve lake-plain reaches had 1–5 yr, and three had < 1 yr of cumulative storage. Among lake-plain reaches, the most storage (6 yr) was upstream of a small (0.4 km2), second-order stream reach. Three glacial-till pasture reaches, each first or second-order streams, had > 10 yr worth of stored sediment. Among other glacial-till sites, four had accumulated 1–3 yr of upstream erosion and five had < 1 yr worth, with less accumulation in streams near the shoreline feature. One grassed waterway (glacial till) and one roadside ditch (lake plain) had no upstream storage.
3.5.2 Proportion of new sediment in bulk streambed sediment using fallout radionuclides
Relative age for twelve RGA bulk streambed-sediment samples ranged from all old to all new (0–100% new sediment). One lake-plain, cropland site had no discernable new sediment (BC17). Two forested sites on the ancient-shoreline transition from glacial till to lake plain had no discernable old sediment (BC18, 21). The median (29% new) was bounded by the largest contributing area and a site on the shoreline feature. Those sites with a mix of sediment age (18–57% new) spanned the range of contributing area, land use, stream order, and ecoregion (Fig. 5).
Streambed-sediment samples identified as mostly sourced from streambank were in the lower range of activity for both FRN (Fig. 5a, underlined sites), with a consistent slope between 7Be and 210Pbxs activity. The proportion of new sediment (Fig. 5b) did not correlate with either stream slope (Fig. 5c) or in-channel storage of streambed sediment (Fig. 5e). There was a general positive correlation to streambank erosion (Fig. 5d), especially for those sites that were mostly streambank-derived sediment, and a negative relation to S:E (Fig. 5f). The proportion of new sediment did not correlate to either the sed-P concentration of the soft, fine-grained streambed sediment (Fig. 5g) or median grain diameter (Fig. 5h).
4 Discussion
After multiple decades focused on field management to mitigate HABs (Annex 4 Task Team 2015; Baker et al. 2019), research has shown in-stream sources of P as an important piece of the puzzle (Jarvie et al. 2013; McDowell et al. 2020; Williamson et al. 2020a; King et al. 2021; Kreiling et al. 2023). This inventory and recency assessment of Black Creek in-channel sediment and associated P differentiated upland and streambank contributions to streambed sediment (Fig. 1), with a mix of recently mobilized sediment and sediment not recently exposed to rainfall (Fig. 5). Together, these data indicate that in-stream accumulation of streambed sediment, even in small watersheds (Fig. 3), has the potential to affect downstream sediment and P loads (Fig. 4) in the Maumee River on a management timescale, delaying successful reductions to Lake Erie.
4.1 Streambed-sediment source, storage, and implications for legacy phosphorus source
Fine-grained material (< 63 μm) was the focus of this sediment inventory because it includes particles most readily transported by streamflow as suspended sediment (Lowrance et al. 2006). Suspended sediment fingerprinted for Black Creek was ≈ 90% fines, with d50 ≈ 4 μm (Williamson et al. 2021a). In contrast, streambed sediment from both glacial till (median = 7 μm) and lake-plain (14 μm) reaches was coarser than previously sampled suspended sediment.
Streambed sediment was significantly coarser than upland sources, and sed-P exceeded that of cropland, forest, and road source samples, but was similar to pasture, streambank, and suspended sediment (Williamson et al. 2020a). This contrasts a similar analysis from a Fox River tributary, another Great-Lakes priority basin, where sed-P from suspended sediment and manure-treated cropland exceeded that of streambank and streambed sediment (Blount et al. 2022). The implication is that the Black Creek in-channel environment, with median base-flow DP = 0.068 mg L−1 (Williamson et al. 2021a), drives similar sed-P for streambed sediment, suspended sediment, and streambank. In 2019, DP concentrations at BC8 exceeded concentrations measured at all other sites in the Maumee River, and BC1, 7, 8 had the three highest DP concentrations in 2021 (78 sites total; Kreiling et al. 2023); these sites were among those with the smallest contributing area. This indicates potential for ongoing sorption and storage of P in streambed sediment and value in understanding headwater-tributary environments.
The potential for streambed sediment to sorb and store P from the water column at 3 of 4 sites is supported by EPC0 and PSR (Table 2); streambank PSR was similar to that for streambed sediment (Fig. 4). While sed-P was distinguishable both as a function of land use and ecoregion in Black Creek source samples, streambed-sediment sed-P did not consistently vary as a function of proximal land use, ecoregion, or d50, even though particle size increased with stream order. This further indicates homogenization of sed-P during sediment transport.
4.2 Recency and environments of streambed-sediment accumulation
Additional evidence of homogenization of sed-P concentrations is the mixed age (18–57% new) of streambed among reaches with similar storage (10–20 Mg km−1; Fig. 5). The consistent relation between 7Be and 210Pbxs reflects a longitudinally consistent process (Matisoff et al. 2005), regardless of stream order and sediment source, with material progressively moving downstream (Verhoff et al. 1979). There was evidence of correlation between proportion of new sediment and streambank erosion, with an inverse relation to S:E, affirming FRN-based relative “age” as time since contact with rain, and that contact with rain can occur during in-network mobilization and transport.
Mixed-age streambed-sediment environments were bracketed by three sites with streambed-sediment storage similar to the median but with proportions of new sediment of either 0 (time since contact with precipitation exceeded 5–12 months) or 1 (moved by most recent event). Among these three sites, streambed sediment was apportioned as a mix of streambank (11–84%), forest (16–38%), and pasture (1–51%); no cropland or road influence was identifiable. At the site with no discernable new sediment (BC17), this indicates that forest-sourced sediment (38%) takes multiple seasons to move through the system, while streambank-sourced sediment (60%), contributed as erosion of the steep-walled channel, is less likely to come into contact with precipitation. This fits with the location of this reach in the stream network: downstream of the ancient shoreline and at the transition to lower stream slope, enabling accumulation, with forested land upstream and a drainage area (4.4 km2) that provides sufficient energy to drive streambank erosion. In contrast, no discernable old sediment indicates recent transport of upland source material, which corresponds to the relatively low storage and small apportionment of streambank (11%) at BC18, reflecting a small contributing area (1.6 km2) and erosional environment upstream from the ancient shoreline. However, at BC21 (2.8 km2), which was similarly situated relative to the shoreline and had no discernable old sediment, 86% of streambed was apportioned as streambank, reflecting streambank erosion that exceeded all but the most downstream site. The implication is that collapsed streambank along smaller streams may be exposed to rainfall when streamflow is below bankfull.
4.3 Differentiating erosional and depositional reaches to guide management
Mean storage and erosion were skewed by individual reaches with high values; median values were lower (6 Mg km−1, 9.8 Mg km−1 yr−1), highlighting the potential of identifying and managing vulnerable sites to reduce transport. Of 25 reaches with visible streambank erosion, 17 indicated an erosional environment (S:E ≤ 1 yr) and eight a depositional environment, where streambed sediment generally accumulated from upstream erosion (S:E > 3 yr). Most sites had evidence of streambed-sediment accumulation from recent upland transport mixed with channel-derived sediment, as has been seen in similar studies (Matisoff et al. 2005; Lamba et al. 2015a; Gellis et al. 2019) and underscoring that suspended and streambed sediment interact. This included the most-downstream reaches (BC1, 3; 33 and 41% new, respectively), where sed-P was relatively low (870–1070 ppm; Fig. 2), reflecting the potential for higher streamflow to limit interaction between the water column DP and accumulated streambed sediment. These fourth-order, erosional reaches had low storage and high erosion, with > 75% of streambed sediment apportioned as streambank (Fig. 1), similar to what was seen previously at BC1 (Williamson et al. 2020a) and in Green Bay tributaries (Fitzpatrick et al. 2019; Blount et al. 2022).
The proximity of streambank to the channel facilitates sediment contribution to streambed, even during summer events, when upland sources are likely less. Upland sediment was discernable at each site; however, sources varied. Only two sites (BC1, 25) had > 3% of streambed sediment apportioned as cropland (23% and 17%, respectively). These sites are at opposite ends of the network, with remaining streambed sediment mostly apportioned as streambank at BC1, but as upland sources (48% pasture, 8% road) at BC25.
Streambed-sediment apportionment as cropland was less than the proportion of contributing area at all sites. This corroborates results from 2017 (BC1, 7, 8; Williamson et al. 2020a) and indicates that cropland-derived sediment is unlikely to settle to streambed but remains in suspension for transport to the receiving stream (the Maumee). Identification of cropland material in suspended sediment further supports this interpretation, although apportionments were consistently exceeded by streambank contributions (BC1, 7, 8; Williamson et al. 2020a).
Some combination of road, pasture, and/or forest was identified in each 2019 streambed-sediment sample, with a general inverse relation to drainage area (Fig. 1). Smaller sites had significantly less streambank and reflected contributing-area land use, similar to studies in other Midwest basins (Williamson et al. 2014; Lamba et al. 2015b; Fitzpatrick et al. 2019). Thus, upland material from non-cropland sources is likely to accumulate as streambed sediment, indicating that management of non-cropland landscape may be integral to addressing long-term sediment and P loads. Road-derived sediment was distinguishable at half of the sites, but had significantly lower P and coarser d50, indicating less potential to contribute to the P load. In contrast, pasture was distinguishable for four of five glacial-till sites and was the source with the highest sed-P and PMeh.
Pasture-derived streambed sediment equates to storage of sed-P and bioavailable P. Pasture also had the highest PSR, in a range indicating release of bioavailable P to the water column. Of the 90-km total Black Creek stream network, 20% traverses active horse pastures (Williamson et al. 2020a) that support an Amish community like those growing in 22 other states (Donnermeyer et al. 2013). Most of these pastures are on highly erodible soils (SNRT Inc. 2015; Porter et al. 2018). Expanding the management strategy for pastures and associated streams could address sediment with the potential to supply both total and bioavailable P to Black Creek, the Maumee, and the WLEB.
In contrast, both cropland and forest samples had relatively low PMeh and PSRs, indicating a potential to sorb DP during transport. This further supports research in the Maumee that P sorption to sediment is slowing bioavailable-P delivery to downstream water bodies (King et al. 2021; Williamson et al. 2021a, b). Black Creek tributaries transition from first- and second-order to third-order streams near the transition from glacial till to lake plain along the ancient Lake Maumee shoreline; similar features occur in other WLEB and Great Lakes basins (Fisher et al. 2015). Forest preservation is common along these transitions, and erosion was higher in forested reaches relative to cropland and pasture reaches (Fig. 3), underscoring that this is likely why these locations are not managed as cropland; this includes reaches in the community of Harlan. The position of forested land in the basin may present an opportunity to develop water-quality related infrastructure or conservation management to mitigate headwater sediment and P, without interfering with agricultural production.
Identifying areas where management of streambed-sediment storage and streambank erosion could be focused may facilitate successful mitigation. This analysis indicates the importance of supplementing basin-wide monitoring with reach-level surveys. Streambank erosion significantly increased with contributing area and stream order, potentially indicating a relation with the accumulation of flow or erosional potential as a function of reach-specific combinations of streamflow, slope, and width of flow in the channel. However, a third-order stream with a small drainage area had one of the highest erosion rates, exceeded only by the most downstream reach, indicating the importance of identifying reaches where the channel intersects geomorphic features that are susceptible to erosion. None of these factors had a significant correlation with in-stream storage, indicating that soil properties, stream characteristics, and land management combine to drive accumulation of streambed sediment.
Fine-grained streambed sediment stored in the Black Creek network (≈ 2200 Mg) potentially holds ≈ 2300 kg sed-P, with the estimate using the median streambed sed-P (2367 kg) similar to that estimated by integrating the source apportionment and median sed-P of individual sources (2248 kg). For context, the annual PP load (TP-DP) was 1293–10,771 kg (water years 2016–2021; median = 4951); the annual suspended-sediment load was 533–7616 Mg (median = 3230 Mg) (USGS 2023). This contrasts with what was measured in a Green Bay tributary, where fine, streambed-sediment storage amounted to 3 yr of modeled suspended-sediment load, but only 20% of annual TP (Blount et al. 2022). That Black Creek streambed-sediment storage equates to two-thirds of the annual suspended-sediment load and half of the annual PP load (20–40% of TP) makes it relevant to WLEB goals of reducing TP by 40% (Annex 4 Task Team 2015). However, these in-channel sources are commonly overlooked or are inadequately represented in basin models of P (Lamba et al. 2016).
Total bioavailable P was more difficult to estimate with available data. We estimated storage of 90 kg PMeh using the median bulk streambed concentrations from all years and 168 kg PMeh using the source apportionment at 13 sites and median source PMeh from bulk source samples. This estimate applies bulk PMeh values to the fine-grained storage volume, with the interpretation that bioavailable P is concentrated in finer particles (Sharpley et al. 1992). These estimates are an order of magnitude less than the annual DP load for Black Creek (1513–3735 kg; median = 2671 kg), almost all of which has the potential to be bioavailable (Baker et al. 2014). However, this underscores that 4–7% of streambed-stored P may be bioavailable.
5 Conclusions
This inventory of in-channel sediment and sed-P sources highlights that managing nutrients that sustain HABs could benefit from improved consideration of the complexities of streambed-sediment storage and addressing streambank erosion as a source of sediment and sed-P. Streambed-sediment sed-P concentrations exceeded those of most upland sources, indicating sorption of DP from the water column to sediment during transport which fosters increased PP through the stream network. This highlights that in-channel sediment storage has implications for the longevity of both DP and PP in this basin and downstream. Streambed-sediment storage equates to storage of sed-P and bioavailable P.
A combination of road, pasture, and/or forest was identified in each 2019 streambed sample, with a general inverse relation to drainage area; first- and second-order streams, most of which were on glacial till, more reflected contributing-area land use. Pasture was distinguishable in most glacial-till streambed sediment and had the highest sed-P and PMeh. Cropland, which was 8–60% of contributing areas, was only identified in three of 13 streambed samples (3–23%); combined with the presence of cropland in suspended sediment analyzed in WY 2018, this indicates that cropland-derived sediment remains in suspension at upstream reaches, with delivery to larger, more shallow-sloped streams. Forest source samples had similar sed-P and PMeh to cropland, and PSR was the lowest of the source types, indicating that this sediment has the potential to sorb P from the water column. These forested reaches commonly marked the transition of glacial till to lake plain, a geomorphic feature that is susceptible to erosion. Consequently, these locations may provide an opportunity to manage sediment, P, and the hydraulic energy that results as contributing area accumulates and the network adjusts to the lake-plain environment.
Larger contributing areas, that included the transition from till to lake plain, had more streambank-derived streambed sediment. Streambed sediment near this transition had no differentiable old sediment, indicating that the low S:E at these sites reflects reworking of sediment and exposure to rainfall when streamflow recedes. Otherwise, streambed sediment was generally a mix of “new” sediment that was recently in contact with rainfall and older streambed sediment, highlighting that this material moves progressively downstream during multiple events.
Data availability
Data are available from U.S. Geological Survey's ScienceBase at citations provided in methods section.
References
Annex 4 Task Team (2015) Recommended phosphorus loading targets for Lake Erie - Annex 4 Objectives and Targets Task Team Final Report to the Nutrients Annex Subcommittee, U.S. Environmental Protection Agency. https://www.epa.gov/sites/production/files/2015-06/documents/report-recommended-phosphorus-loading-targets-lake-erie-201505.pdf
Baker DB, Confesor R, Ewing DE, Johnson LT, Kramer JW, Merryfield BJ (2014) Phosphorus loading to Lake Erie from the Maumee, Sandusky and Cuyahoga rivers: the importance of bioavailability. J Great Lakes Res 40:502–517. https://doi.org/10.1016/j.jglr.2014.05.001
Baker DB, Johnson LT, Confesor RB, Crumrine JP, Guo T, Manning NF (2019) Needed: early-term adjustments for Lake Erie phosphorus target loads to address western basin cyanobacterial blooms. J Great Lakes Res 45:203–211. https://doi.org/10.1016/j.jglr.2019.01.011
Benjamini Y, Hochberg Y (1995) Controlling the false discovery rate: a practical and powerful approach to multiple testing. J R Stat Soc. Series B (Methodological) 57:289–300. http://www.jstor.org/stable/2346101
Blount JD, Lenoch LEK, Fitzpatrick FA (2022) Stream corridor and upland sources of fluvial sediment and phosphorus from a mixed urban-agricultural tributary to the Great Lakes. J Great Lakes Res 48:1536–1549. https://doi.org/10.1016/j.jglr.2022.08.024
Blount JD, Fitzpatrick FA, Williamson TN (2021) Black Creek Rapid Geomorphic Assessment, Allen County, Indiana, U.S. Geological Survey data release. https://doi.org/10.5066/P9F1LQ6H
Boudreault M, Koiter AJ, Lobb DA, Liu K, Benoy G, Owens PN, Li S (2019) Comparison of sampling designs for sediment source fingerprinting in an agricultural watershed in Atlantic Canada. J Soils Sediments 19:3302–3318. https://doi.org/10.1007/s11368-019-02306-6
Bremner JM, Tabatabai MA (1971) Use of automated combustion techniques for total carbon, total nitrogen, and total sulfur analysis of soils, Instrumental Methods for Analysis of Soils and Plant Tissue, pp. 1–15
Capel PD, McCarthy KA, Coupe RH, Grey KM, Amenumey SE, Baker NT, Johnson RL (2018a) Agriculture — A river runs through it — The connections between agriculture and water quality. US Geolog Survey Circ 1433. https://doi.org/10.3133/cir1433
Capel PD, Wolock DM, Coupe RH, Roth JL (2018b) A conceptual framework for effectively anticipating water-quality changes resulting from changes in agricultural activities. US Geolog Survey Sci Investig Rep 2017–5095. https://doi.org/10.3133/sir20175095
Cashman MJ, Gellis A, Gorman Sanisaca L, Noe G, Cogliandro V, Baker A (2018) Bank-derived material dominates fluvial sediment in a suburban Chesapeake Bay watershed. River Res App 34:1032–1044. https://doi.org/10.1002/rra.3325
Casillas-Ituarte NN, Sawyer AH, Danner KM, King KW, Covault AJ (2020) Internal phosphorus storage in two headwater agricultural streams in the Lake Erie Basin. Environ Sci Technol 54:176–183. https://doi.org/10.1021/acs.est.9b04232
Collins AL, Walling DE, Webb L, King P (2010) Apportioning catchment scale sediment sources using a modified composite fingerprinting technique incorporating property weightings and prior information. Geoderma 155:249–261. https://doi.org/10.1016/j.geoderma.2009.12.008
Collins AL et al (2020) Sediment source fingerprinting: benchmarking recent outputs, remaining challenges and emerging themes. J Soils Sediments 20:4160–4193. https://doi.org/10.1007/s11368-020-02755-4
Donnermeyer J, Anderson C, Cooksey E (2013) The Amish Population: county estimates and settlement patterns. Amishstudies 1:72–109. https://ideaexchange.uakron.edu/amishstudies/vol1/iss1/4/
Durner W, Iden SC, von Unold G (2017) The integral suspension pressure method (ISP) for precise particle-size analysis by gravitational sedimentation. Water Resour Res 53:33–48. https://doi.org/10.1002/2016WR019830
Fisher T, Blockland JD, Anderson B, Krantz DE, Stierman DJ, Goble R (2015) Evidence of sequence and age of Ancestral Lake Erie lake-levels, northwest Ohio. Ohio J Sci 115:62–78. https://doi.org/10.18061/ojs.v115i2.4614
Fitzpatrick FA, Ellison CA, Czuba CR, Young BM, McCool MM, Groten JT (2016) Geomorphic responses of Duluth-area streams to the June 2012 flood, Minnesota. US Geolog Survey Sci Investig Rep 2016–5104. https://doi.org/10.3133/sir20165104
Fitzpatrick FA, Blount J, Kammel L, Francart S, Gellis A, Eikenberry B (2019) Instream sources of suspended sediment and phosphorus from an agricultural tributary to the Great Lakes, Federal Interagency Sedimentaton and Hydrologic Modeling Conference, Reno, NV, pp. 15. https://pubs.er.usgs.gov/publication/70217015
Foote KJ, Joy MK, Death RG (2015) New Zealand dairy farming: milking our environment for all its worth. Environ Manage 56:709–720. https://doi.org/10.1007/s00267-015-0517-x
Gellis AC, Gorman Sanisaca L (2018) Sediment fingerprinting to delineate sources of sediment in the agricultural and forested Smith Creek Watershed, Virginia, USA. J Am Water Resour Assoc 54:1197–1221. https://doi.org/10.1111/1752-1688.12680
Gellis A, Noe G (2013) Sediment source analysis in the Linganore Creek watershed, Maryland, USA, using the sediment fingerprinting approach: 2008 to 2010. J Soils Sediments 13:1735–1753. https://doi.org/10.1007/s11368-013-0771-6
Gellis AC, Fuller CC, Van Metre P, Filstrup CT, Tomer MD, Cole KJ, Sabitov TY (2019) Combining sediment fingerprinting with age-dating sediment using fallout radionuclides for an agricultural stream, Walnut Creek, Iowa, USA. J Soils Sediments 19:3374–3396. https://doi.org/10.1007/s11368-018-2168-z
Gellis AC, Walling DE (2013) Sediment source fingerprinting (tracing) and sediment budgets as tools in targeting river and watershed restoration programs, stream restoration in dynamic fluvial systems. American Geophysical Union, pp. 263–291. https://doi.org/10.1029/2010gm000960
Gellis AC, Noe GB, Clune JB, Myers MK, Hupp CR, Schenk E, Schwarz G (2014) Sources of fine-grained sediment in Linganore Creek watershed, Maryland: 2008 to 2010, U.S. Geological Survey Scientific Investigations Report 2014–5147. https://doi.org/10.3133/sir20145147
Gorman Sanisaca LE, Gellis AC, Lorenz DL (2017) Determining the sources of fine-grained sediment using the Sediment Source Assessment Tool (Sed_SAT). U.S. Geological Survey Open File Report 2017–1062. https://doi.org/10.3133/ofr20171062
Guzmán G, Quinton JN, Nearing MA, Mabit L, Gómez JA (2013) Sediment tracers in water erosion studies: current approaches and challenges. J Soils Sediments 13:816–833. https://doi.org/10.1007/s11368-013-0659-5
Haggard BE, Smith DR, Brye KR (2007) Variations in stream water and sediment phosphorus among select Ozark catchments. J Environ Qual 36:1725–1734. https://doi.org/10.2134/jeq2006.0517
Han H, Allan JD, Bosch NS (2012) Historical pattern of phosphorus loading to Lake Erie watersheds. J Great Lakes Res 38:289–298. https://doi.org/10.1016/j.jglr.2012.03.004
Hankins R (2023) Investigating the use of fallout radionuclides beryllium-7 and excess lead-210 as short-term stream sediment chronometers in the agricultural upper midwest, USA. Masters Thesis, University of Minnesota
Homer C, Dewitz J, Jin S, Xian G, Costello C, Danielson P, Gass L, Funk M, Wickham J, Stehman S, Auch R, Riitters K (2020) Conterminous United States land cover change patterns 2001–2016 from the 2016 National Land Cover Database. ISPRS J Photogramm Remote Sens 162:184–199. https://doi.org/10.1016/j.isprsjprs.2020.02.019
Huisman NLH, Karthikeyan KG, Lamba J, Thompson AM, Peaslee G (2013) Quantification of seasonal sediment and phosphorus transport dynamics in an agricultural watershed using radiometric fingerprinting techniques. J Soils Sediments 13:1724–1734. https://doi.org/10.1007/s11368-013-0769-0
Jarvie HP, Sharpley AN, Spears B, Buda AR, May L, Kleinman PJA (2013) Water quality remediation faces unprecedented challenges from “legacy phosphorus.” Environ Sci Technol 47:8997–8998. https://doi.org/10.1021/es403160a
Karwan DL, Siegert CM, Levia DF, Pizzuto J, Marquard J, Aalto R, Aufdenkampe AK (2016) Beryllium-7 wet deposition variation with storm height, synoptic classification, and tree canopy state in the mid-Atlantic USA. Hydrol Process 30:75–89. https://doi.org/10.1002/hyp.10571
Karwan DL, Pizzuto JE, Aalto R, Marquard J, Harpold A, Skalak K, Benthem A, Levia DF, Siegert CM, Aufdenkampe AK (2018) Direct channel precipitation and storm characteristics influence short-term fallout radionuclide assessment of sediment source. Water Resour Res 54:4579–4594. https://doi.org/10.1029/2017WR021684
Karwan DL, Williamson TN (2023) Fallout-radionuclide activity in samples collected from fine-grained, streambed sediment in the Black Creek, Indiana stream-channel network, 2019, U.S. Geological Survey data release. https://doi.org/10.5066/P9L5P7BZ
Kast JB, Apostel AM, Kalcic MM, Muenich RL, Dagnew A, Long CM, Evenson G, Martin JF (2021) Source contribution to phosphorus loads from the Maumee River watershed to Lake Erie. J Environ Manage 279:111803. https://doi.org/10.1016/j.jenvman.2020.111803
King WM, Curless SE, Hood JM (2021) River phosphorus cycling constrains lake cyanobacteria blooms. bioRxiv, 2021.05.03.442426. https://doi.org/10.1101/2021.05.03.442426
Kreiling RM, Thoms MC, Bartsch LA, Richardson WB, Christensen VG (2019) Complex response of sediment phosphorus to land use and management within a river network. J Geophys Res Biogeosci 124:1764–1780. https://doi.org/10.1029/2019JG005171
Kreiling RM, Bartsch LA, Perner PM, Breckner KJ (2022) Great Lakes Restoration Initiative: nutrient cycling in riverbed sediment in the Maumee River Basin, 2019 and 2021 Data, U.S. Geological Survey Data Release. https://doi.org/10.5066/P9OMM51R
Kreiling RM, Perner PM, Breckner KJ, Williamson TN, Bartsch LA, Hood JM, Manning NF, Johnson LT (2023) Watershed- and reach-scale drivers of phosphorus retention and release by streambed sediment in a western Lake Erie watershed during summer. Sci Total Environ, 160804. https://doi.org/10.1016/j.scitotenv.2022.160804
Kwan H, Swanson S (2014) Prediction of annual streambank erosion for Sequoia National Forest, California. JAWRA J Am Water Resour Assoc 50:1439–1447. https://doi.org/10.1111/jawr.12200
Lamba J, Karthikeyan KG, Thompson AM (2015a) Using radiometric fingerprinting and phosphorus to elucidate sediment transport dynamics in an agricultural watershed. Hydrol Process 29:2681–2693. https://doi.org/10.1002/hyp.10396
Lamba J, Thompson AM, Karthikeyan KG, Fitzpatrick FA (2015b) Sources of fine sediment stored in agricultural lowland streams, Midwest, USA. Geomorphology 236:44–53. https://doi.org/10.1016/j.geomorph.2015.02.001
Lamba J, Thompson AM, Karthikeyan KG, Panuska JC, Good LW (2016) Effect of best management practice implementation on sediment and phosphorus load reductions at subwatershed and watershed scale using SWAT model. Int J Sediment Res 31:386–394. https://doi.org/10.1016/j.ijsrc.2016.06.004
Lowrance R, Isenhart TM, Gburek WJ, FD Shields J, PJ Wigington J, Dabney SM (2006) Landscape management practices. In: Schnepf M, Cox C (Eds). Soil Water Conserv Soc. 271–317
Mabit L, Benmansour M, Abril JM, Walling DE, Meusburger K, Iurian AR, Bernard C, Tarján S, Owens PN, Blake WH, Alewell C (2014) Fallout 210Pb as a soil and sediment tracer in catchment sediment budget investigations: a review. 138:335–351. https://doi.org/10.1016/j.earscirev.2014.06.007
Matisoff G, Wilson CG, Whiting PJ (2005) The 7Be/210Pbxs ratio as an indicator of suspended sediment age or fraction new sediment in suspension. Earth Surf Process Landforms 30:1191–1201. https://doi.org/10.1002/esp.1270
McDowell RW, Depree C, Stenger R (2020) Likely controls on dissolved reactive phosphorus concentrations in baseflow of an agricultural stream. J Soils Sediments 20:3254–3265. https://doi.org/10.1007/s11368-020-02644-w
Mehlich A (1984) Mehlich 3 soil test extractant: a modification of Mehlich 2 extractant. Commun Soil Sci Plant Anal 15:1409–1416. https://doi.org/10.1080/00103628409367568
Moriasi DN, Duriancik LF, Sadler EJ, Tsegaye T, Steiner JL, Locke MA, Strickland TC, Osmond DL (2020) Quantifying the impacts of the Conservation Effects Assessment Project watershed assessments: the first fifteen years. J Soil Water Conserv 75:57A-74A. https://doi.org/10.2489/jswc.75.3.57A
Nair VD (2014) Soil phosphorus saturation ratio for risk assessment in land use systems. Frontiers Environ Sci 2. https://doi.org/10.3389/fenvs.2014.00006
National Oceanic and Atmospheric Administration [NOAA] (2023) U.S. Daily Climate Normals (1991–2020) Fort Wayne Area, IN Annual Assessment. Natl Oceanic Atmos Admin. https://www.weather.gov/wrh/climate?wfo=iwx
Newbold JD, Elwood JW, O’Neill RV, Sheldon AL (1983) Phosphorus dynamics in a woodland stream ecosystem: a study of nutrient spiralling. Ecology 64:1249–1265. https://doi.org/10.2307/1937833
Omernik JM, Griffith GE (2014) Ecoregions of the conterminous United States: evolution of a hierarchical spatial framework. Environ Manage 54:1249–1266. https://doi.org/10.1007/s00267-014-0364-1
Osmond D, Meals D, Hoag D, Arabi M, Luloff A, Jennings G, McFarland M, Spooner J, Sharpley A, Line D (2012) Improving conservation practices programming to protect water quality in agricultural watersheds: lessons learned from the National Institute of Food and Agriculture-Conservation Effects Assessment Project. J Soil Water Conserv 67:122A-127A. https://doi.org/10.2489/jswc.67.5.122A
Palmer-Felgate EJ, Jarvie HP, Withers PJA, Mortimer RJG, Krom MD (2009) Stream-bed phosphorus in paired catchments with different agricultural land use intensity. Agr Ecosyst Environ 134:53–66. https://doi.org/10.1016/j.agee.2009.05.014
Perner P, Williams CO, Williamson TN (2022) Mehlich-III extractable data for sediment source fingerprinting of suspended and bottom sediment in Black Creek, Indiana, tributary to the Maumee River and western Lake Erie - source samples, U.S. Geological Survey data release. https://doi.org/10.5066/P9W28HF0
Porter SA, Tomer MD, James DE, VanHorn JD (2018) Agricultural Conservation Planning Framewor ArcGIS Toolbox User’s Manual. National Laboratory for Agriculture and the Environment, USDA-ARS, Ames, IA. https://doi.org/10.15482/USDA.ADC/1171155
R Core Team (2022) R: a language and environment for statistical computing. R Foundation for Statistical Computing., Vienna, Austria. http://www.R-project.org/
Robertson DM, Saad DA (2011) Nutrient inputs to the Laurentian Great Lakes by source and watershed estimated using SPARROW watershed models. J Am Water Resour Assoc 47:1011–1033. https://doi.org/10.1111/j.1752-1688.2011.00574.x
Scavia D, Kalcic M, Muenich RL, Read J, Aloysius N, Bertani I, Boles C, Confesor R, DePinto J, Gildow M, Martin J, Redder T, Robertson D, Sowa S, Wang Y-C, Yen H (2017) Multiple models guide strategies for agricultural nutrient reductions. Front Ecol Environ 15:126–132. https://doi.org/10.1002/fee.1472
Schilling KE, Isenhart TM, Wolter CF, Streeter MT, Kovar JL (2022) Contribution of streambanks to phosphorus export from Iowa. J Soil Water Conserv 77:103–112. https://doi.org/10.2489/jswc.2022.00036
Sharpley AN, Smith SJ, Jones OR, Berg WA, Coleman GA (1992) The transport of bioavailable phosphorus in agricultural runoff. J Environ Qual 21:30–35. https://doi.org/10.2134/jeq1992.00472425002100010003x
Simpson ZP, McDowell RW, Condron LM, McDaniel MD, Jarvie HP, Abell JM (2021) Sediment phosphorus buffering in streams at baseflow: a meta-analysis. J Environ Qual 50:287–311. https://doi.org/10.1002/jeq2.20202
SNRT Inc. Natural Resource Group in cooperation with Allen County and Defiance County Soil and Water Conservation Districts [SNRT-ACSWCD] (2015) Upper Maumee River Waterhsed Managment Plan - HUC 0410005, Upper Maumee River Waterhsed Project Steering Committee. Indiana Dept Environ Manag. https://www.in.gov/idem/nps/resources/watershed-management-plans/maumee-river-upper-wmp-2-21/
Stackpoole SM, Stets EG, Sprague LA (2019) Variable impacts of contemporary versus legacy agricultural phosphorus on US river water quality. Proc Natl Acad Sci 116:20562–20567. https://doi.org/10.1073/pnas.1903226116
Standard Methods: American Public Health Association, American Water Works Association, Water Environment Federation (2021) 4500-P PHOSPHORUS, Standard Methods For the Examination of Water and Wastewater.
Strahler AN (1957) Quantitative analysis of watershed geomorphology. EOS Trans Am Geophys Union 38:913–920. https://doi.org/10.1029/TR038i006p00913
Tufekcioglu M, Isenhart TM, Schultz RC, Bear DA, Kovar JL, Russell JR (2012) Stream bank erosion as a source of sediment and phosphorus in grazed pastures of the Rathbun Lake Watershed in southern Iowa. United States J Soil Water Conserv 67:545–555. https://doi.org/10.2489/jswc.67.6.545
US Department of Agriculture - Natural Resources Conservation Service [USDA-NRCS] Wisconsin (2015) Wisconsin Field Office Technical Guide - Section III, Streambank Erosion, Wisconsin. https://efotg.sc.egov.usda.gov/#/state/WI/documents
US Department of Agriculture - Natural Resources Conservation Service [USDA-NRCS] (2020) Web Soil Survey - gSSURGO. Natural Resources Conservation Service, United States Department of Agriculture. http://websoilsurvey.nrcs.usda.gov/
US Department of Agriculture - Natural Resource Conservation Service [USDA-NRCS] (2016) Soil Survey Geographic (SSURGO) Database for Allen County, IN. Soil Survey Staff Natural Res Conserv Service, United States Dept Agric. https://websoilsurvey.sc.egov.usda.gov/App/WebSoilSurvey.aspx
US Department of Agriculture - Natural Resource Conservation Service [USDA-NRCS] (2017) Conservation practice adoption on cultivated cropland acres: effects on instream nutrient and sediment dynamics and delivery in western Lake Erie Basin, 2003–06 and 2012. https://www.nrcs.usda.gov/publications/ceap-crop-2017-Nutrient-Sediment-full.pdf
US Environmental Protection Agency [USEPA] (1996) Method 6010B, Inductively Couple d Plasma-Atomic Emission Spectrometry, USEPA. https://www.epa.gov/sites/default/files/documents/6010b.pdf
US Geological Survey [USGS] (2020) USGS National Geospatial Program National Hydrography Dataset Plus High Resolution Resolution (NHDPlus HR) for 4-digit Hydrologic Units. https://apps.nationalmap.gov/downloader/#/
US Geological Survey (2023) USGS water data for the Nation: U.S. Geological Survey National Water Information System database. https://doi.org/10.5066/F7P55KJN
Verhoff FH, Melfi DA, Yaksich SM (1979) Storm travel distance calculations for total phosphorus and suspended materials in rivers. Water Resour Res 15:1354–1360. https://doi.org/10.1029/WR015i006p01354
Williamson TN, Christensen VG, Richardson WB, Frey JW, Gellis AC, Kieta KA, Fitzpatrick FA (2014) Stream sediment sources in midwest agricultural basins with land retirement along channel. J Environ Qual 43:1624–1634. https://doi.org/10.2134/jeq2013.12.0521
Williamson TN, Dobrowolski ED, Gellis AC, Sabitov T, Saniasca LG (2020a) Monthly suspended-sediment apportionment for a western Lake Erie agricultural tributary. J Great Lakes Res 46:1307–1320. https://doi.org/10.1016/j.jglr.2020.06.011
Williamson TN, Dobrowolski EG, Kreiling RM (2021a) Phosphorus sources, forms, and abundance as a function of streamflow and field conditions in a Maumee River tributary, 2016–2019. J Environ Qual 52:492–507. https://doi.org/10.1002/jeq2.20290
Williamson TN, Hoefling DJ (2023) Chemical and physical data for sediment source tracking of streambed sediment in Black Creek, Indiana, tributary to the Maumee River and western Lake Erie - 2019, U.S. Geological Survey data release. https://doi.org/10.5066/P9ATF9P8
Williamson TN, Hardebeck MJ, Martin GR (2020b) Chemical and physical data for sediment source fingerprinting of suspended and bottom sediment in Black Creek, Indiana, tributary to the Maumee River and western Lake Erie - fluvial-target samples, U.S. Geological Survey Data Release. https://doi.org/10.5066/P9EOEFOL
Williamson TN, Hardebeck MJ, Martin GR (2020c) Chemical and physical data for sediment source fingerprinting of suspended and bottom sediment in Black Creek, Indiana, tributary to the Maumee River and western Lake Erie - source samples, U.S. Geological Survey Data Release. https://doi.org/10.5066/P9W28HF0
Williamson TN, Shaffer KH, Runkle DL, Hardebeck MJ, Dobrowolski EG, Frey JW, Baker NT, Collier KM, Huitger CA, Kula SP, Haefner RJ, Hartley LM, Crates HF, Finnegan DP, Reithel NJ, Toussant CA, Weaver TL (2021b) Nutrient and suspended-sediment concentrations in the Maumee River and tributaries during 2019 rain-induced fallow conditions. J Great Lakes Res 47. https://doi.org/10.1016/j.jglr.2021.10.004
Withers PJA, Jarvie HP (2008) Delivery and cycling of phosphorus in rivers: a review. Sci Total Environ 400:379–395. https://doi.org/10.1016/j.scitotenv.2008.08.002
Acknowledgements
This work was done in cooperation with the Great Lakes Restoration Initiative. Diana Karwan was partially supported by U.S. Department of Agriculture Forest Service and the Minnesota Agricultural Experiment Station (MN-042). We appreciate the help of the Allen County, Indiana Soil and Water Conservation District, and Black Creek community in facilitating access to field sites. We are grateful to members of the University of Minnesota Watershed-Hydrology Lab who helped prepare and run fallout radionuclide samples. We also thank the many U.S. Geological Survey staff who helped collect and process the samples. Any use of trade, firm, or product names is for descriptive purposes only and does not imply endorsement by the U.S. Government.
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Williamson, T.N., Fitzpatrick, F.A., Kreiling, R.M. et al. Sediment budget of a Maumee River headwater tributary: how streambank erosion, streambed-sediment storage, and streambed-sediment source inform our understanding of legacy phosphorus. J Soils Sediments 24, 1447–1463 (2024). https://doi.org/10.1007/s11368-023-03713-6
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DOI: https://doi.org/10.1007/s11368-023-03713-6