Understanding Dissolved Organic Matter Biogeochemistry Through <em>In Situ</em> Nutrient Manipulations in Stream Ecosystems

Adam S. Wymore; Bianca Rodr&#237;guez-Cardona; William H. McDowell

doi:10.3791/54704

JoVE Journal > Environment

Ambiente

Understanding Dissolved Organic Matter Biogeochemistry Through In Situ Nutrient Manipulations in Stream Ecosystems

Published: October 29, 2016

doi:

10.3791/54704

Adam S. Wymore¹, Bianca Rodríguez-Cardona¹, William H. McDowell¹

¹Department of Natural Resources and the Environment,University of New Hampshire

Summary

Dissolved organic matter provides an important source of energy and nutrients to stream ecosystems. Here we demonstrate a field-based method to manipulate the ambient pool of dissolved organic matter in situ through easily replicable nutrient pulses.

Abstract

Dissolved organic matter (DOM) is a highly diverse mixture of molecules providing one of the largest sources of energy and nutrients to stream ecosystems. Yet the in situ study of DOM is difficult as the molecular complexity of the DOM pool cannot be easily reproduced for experimental purposes. Nutrient additions to streams however, have been shown to repeatedly alter the in situ and ambient DOM pool. Here we demonstrate an easily replicable field-based method for manipulating the ambient pool of DOM at the ecosystem scale. During nutrient pulse experiments changes in the concentration of both dissolved organic carbon and dissolved organic nitrogen can be examined across a wide-range of nutrient concentrations. This method allows researchers to examine the controls on the DOM pool and make inferences regarding the role and function that certain fractions of the DOM pool play within ecosystems. We advocate the use of this method as a technique to help develop a deeper understanding of DOM biogeochemistry and how it interacts with nutrients. With further development this method may help elucidate the dynamics of DOM in other ecosystems.

Introduction

Dissolved organic matter (DOM) provides an important energy and nutrient source to freshwater ecosystems and is defined as organic matter that passes through a 0.7 µm filter. Within aquatic ecosystems, DOM can also influence light attenuation and metal complexation. DOM is a highly diverse and heterogeneous mixture of organic compounds with various functional groups, as well as essential nutrients such as nitrogen (N) and phosphorous (P). While the term "DOM" describes the entire pool including its C, N and P components, its concentration is measured as dissolved organic carbon (DOC). The inherent molecular complexity of the DOM pool however, creates challenges to its study. For example, there is no direct way to measure the fraction of the total DOM pool comprised of organic nutrients such as dissolved organic nitrogen (DON) and dissolved organic phosphorus (DOP). Instead, the concentration of organic nutrients must be determined by difference (e.g. [DON] = [total dissolved nitrogen] – [dissolved inorganic nitrogen]).

Adding a realistic DOM amendment to a stream is difficult due to the diversity of the ambient DOM pool. Previous studies have added single carbon sources (e.g. glucose, urea¹)or a particular source such as leaf litter leachate² to manipulate concentrations in the field. However, these sources are not particularly representative of the ambient DOM pool. Trying to refine or concentrate ambient DOM for subsequent experimentation is also wrought with difficulties including the loss of certain fractions (e.g. highly labile components) during processing. As a result, it is difficult to understand the controls on the ambient DOM pool as we currently do not possess any method to directly manipulate the ambient DOM pool. However, since the biogeochemistry of DOM is linked to nutrients commonly found in the environment (e.g. nitrate [NO₃^–]³), we can add other solutes to stream ecosystems and measure the response of the DOM pool to these manipulations. By examining how the DOM pool responds to a wide range of experimentally imposed nutrient concentrations we hope to gain better insight into how DOM responds to fluctuating environmental conditions.

One method commonly used in stream biogeochemistry is the nutrient addition method. Nutrient addition experiments have traditionally been used to understand uptake kinetics or the fate of the added solute^4,5,6,7. Nutrient additions can be short-term on the hr⁶ to day scale⁴, or longer-term manipulations over the course of multiple years⁸. Nutrient additions can also include isotopically labelled nutrients (e.g. ¹⁵N-NO₃^–) to trace added nutrient through biogeochemical reactions. However, isotope-based studies are often expensive and require challenging analyses (e.g. digestions) of the multiple benthic compartments where isotopically-labeled nutrients may be retained. Recent experimentation has revealed the utility of short-term nutrient pulses to elucidate the controls on non-added and ambient solutes such as DOM^9,10, revealing a new way by which to examine real-time in situ biogeochemical reactions. Here we describe and demonstrate the key methodological steps to conducting short-term nutrient pulses with the objective of understanding the coupled biogeochemistry of C and N and specifically the controls on the highly diverse DOM pool. This easily reproducible method involves adding a nutrient pulse to an experimental stream reach and measuring changes in the concentration of both the manipulated solute and the response variable of interest (e.g. DOC, DON, DOP). By directly manipulating nutrient concentrations in situ we are able to indirectly alter the DOM pool and examine how DOM concentration changes across a dynamic range of nutrient concentrations¹⁰.

Protocol

1. Identifying and Characterizing the Ideal Experimental Stream Reach

Ensure that experimental stream reaches are long enough to promote complete mixing of solutes¹¹ and long enough where biological uptake can occur. Reach lengths can vary among streams and experiments. In small first-order headwater streams, reach length may vary from 20-150 m (or longer if the system requires it) depending on discharge and other physical properties of the stream.
1. Exclude large pools from experimental reaches, as they retard the downstream movement of solutes, minimal flow sections, and tributaries that dilute the added solution. Times of low discharge may require shortening the reach length while higher discharge may require a longer reach.
2. Identify a location at the top of the experimental stream reach above a riffle to facilitate mixing of the added solutes. This will be the addition site. At the bottom of the experimental stream reach, identify a location where flow is constricted and representative of about 90% of the total flow (Figure 1). This will be the sample collection site.

Figure 1: Example of Downstream Sampling Site. An ideal sampling site is where the majority of flow is constricted and easily accessible without disturbance of the stream channel and benthos. Here a fallen piece of wood debris has created this sampling point in a small first-order headwater stream. Please click here to view a larger version of this figure.

Obtain discharge measurement and background nutrient concentrations of the solutes of interest prior to experiments in order to calculate the mass of solutes needed for the manipulations. Please see calculations in step 2.2.1.
1. Obtain background concentration data for the target solute of manipulation (e.g. NO₃^–) and chloride (Cl^–) which is often used as the conservative tracer. Use the conservative tracer in the context of these experiments, to track changes in conductivity, which indicate the arrival of the nutrient pulse at the sampling station and the rate in which the pulse is passing through. Conductivity, or specific conductance, is a surrogate for in-situ changes in concentration of the conservative tracer.
2. Characterize the physio-chemical properties of the experimental reach by collecting ancillary data such as reach width and depth, temperature, pH and dissolved oxygen.
  1. Perform measurements that cannot be made with the use of an environmental probe (e.g. width and depth), the day before or immediately after the experiment in order to minimize any benthic or chemical disturbance within the stream channel. Divide the experimental reach in equidistant transects (e.g. every 10 m) where width and at least 3 depth measurements can be assessed (e.g. right bank, thalweg, and left bank). These data are valuable to connect the physical properties of a stream to biogeochemical measurements and if the researchers are also interested in calculating nutrient uptake kinetics and parameters⁶.

2. Preparation for Experiment

Determine the mass (kg) of solute required for manipulation using the outlined equations below.
Note: The example below applies to a nitrate-based experiment with NO₃^– in the form of sodium nitrate (NaNO₃) and assumes a targeted increase of 3x above background (equations are based on those of Kilpatrick and Cobb¹²). In this example the following assumptions have been made with respect to background conditions: discharge = 10 L/sec; [Cl] = 10 mg/L; [NO₃^–] = 50 µg N/L. Due to variation among experiments, adjust required input data.
1. Calculate the Targeted increase (Equation 1):
  Targeted [NO₃– μg N/L] increase = expected background [NO₃– μg N/L] * targeted increase
  150 μg N/L = 50 μg N/L * 3
2. Calculate the total atomic mass flux (Equation 2):
  Total atomic mass flux (NO₃– μg N) = 30 min * 60 sec * Q(L/sec) * targeted [NO₃– μg N/L] increase
  Where 30 minutes is the assumed duration of solute peak¹² and Q is discharge
  2 700 000 μg N = 30 min * 60 sec * 10 L/s * 150 μg N/L
3. Calculate the total molecular mass flux (Equation 3):
  Total molecular mass flux (NO₃– μg N) = total atomic mass flux (NO₃– μg N)/atomic mass (14) * molecular weight (85)
  Where atomic mass refers to N and molecular weight refers to NaNO₃.
  16,392,857.14 μg N = 2,700,000 μg N/(14 * 85)
4. Calculate the mass to add (Equation 4):
  Mass to add (g) = total molecular mass flux (NO₃– μg N)/1,000,000 g/μg
  16.39 g NaNO₃ = 16,392,857.14 μg N/1,000,000 g/μg
  Note: Follow the above calculations for any other solutes including the conservative tracer (e.g. sodium chloride). Make sure to adjust the atomic and molecular masses for the solute of interest.
Prepare all solutes one day prior to field experiments. Weigh out enough solutes to raise the ambient concentration of both the biological tracer and the conservative tracer three times (or desired amount) above background. It is important that the quantity of added solutes causes a measureable change above background concentration that is sufficient to create a wide dynamic range in added nutrient concentration.
1. Weigh solutes using analytical scales and subsequently store in clean acid-washed high-density polyethylene bottles with appropriate labels. Examples of biological tracers include: NO₃^–: sodium nitrate (NaNO₃); NH₄⁺: ammonium chloride (NH₄Cl); PO₄^-3: potassium phosphate (K₂HPO₄). However, the choice of biological tracer will be a function of the biogeochemical question being asked. Options for conservative tracers include sodium chloride (NaCl) and sodium bromide (NaBr).
Collect remaining materials: field book, labeling tape and pen, field measuring tape, cooler, conductivity meter, ~ 20 L bucket and large stirring rod (e.g. beer paddle, rebar, large stick), approximately 50 clean and acid-washed 125 ml high-density polyethylene bottles. Label the 125 ml bottles #1-50.
Note: Less than 50 samples can be taken per experiment and background samples are included in the 50 total bottles.
Optional: Depending on the numbers of field personnel, perform sample filtering on-site (see section #5). If this option is chosen, bring 50 clean, pre-labeled and acid-washed 60 ml high-density polyethylene bottles into the field. Label the 60 ml bottles #1-50 to match the 125 ml collection bottles.

3. Day of Set Up

Deploy the field conductivity meter at the collection site. Place the instrument upstream (approximately 0.5-1.0 m) of where samples will be taken so sample collection does not interfere with instrument readings. The meter will remain in place throughout the experiment. A field conductivity meter is best as it provides real-time conductivity readings, which are required to determine the sampling rate (see step 5.2) and filtration and analysis order (steps 5.3 and 6.1).
Collect 125 ml background samples in triplicate at the addition site and at the collection site of the experimental reach prior to the addition of the solution. These data will be used to verify day-of ambient concentration and to determine variation in solute concentration along the stream reach. These data are also valuable to connect ambient stream chemistry (e.g. DOC: NO₃^– ratios¹³) to the biogeochemical measurements of interest.
Record the time and conductivity of background samples collected.
Record the background conductivity of stream prior to addition of solutions.

4. Adding Solutes

Pour all reagents (16.39 g NaNO₃ and 1483 g NaCl) into a large container (e.g. 20 L bucket) and add enough stream water to completely dissolve the solutes. Rinse reagent vessels thrice with additional stream water and pour rinse into solution container. Keep track of amount of water added.
1. For example, use a 500 ml bottle to pour stream water into the container. Stir solution until all reagents have been completely dissolved.
Collect 60 ml aliquot of the addition solution. Keep this highly concentrated sample separate (e.g. zip-lock bag) from all other samples to minimize cross contamination. Such samples are important if calculating nutrient uptake kinetics⁶ is an additional goal of the research project as these samples can be used to determine the exact mass of solutes added.
Pour solution into addition site. Do this by pouring the solution in a smooth and quick motion to minimize travel lag time and splashing that could reduce the amount of reagents added. Rinse the container and the stir stick three times in the stream immediately after the addition to guarantee all reagents have been added to the stream.
1. Record the time the solution was added: hr:min:sec.
2. Record the masses of tracers added (e.g. NaNO₃ and NaCl).
3. After the solution has been added, do not disturb the stream. Make sure that all travel along the stream occurs on the banks to ensure that the stream benthos and the solution itself are not disturbed.

5. Field Sampling

Order sampling bottles in ascending order while waiting for solution to arrive to the sampling location. Travel time will be a function of discharge and reach length and can be determined ahead of time (one-day prior) either with a NaCl-only injection or rhodamine dye (which can be used to establish travel time¹⁴).
Note: If working on a DON-themed project, avoid using rhodamine dye as it is a type of DON and will therefore alter the ambient DON pool if any remains in the study reach.

Figure 2: Example Schematic of Solute Breakthrough Curve (BTC). A BTC represents changes in solute concentration over time and can be used to explain the transit and biogeochemical cycling of a tracer in a stream. Grab samples should be taken across the BTC with a frequency that gives equal representation to both the ascending and descending limbs of the BTC. Please click here to view a larger version of this figure.

Sample Collection
Note: The over-arching objective of sample collection, is to adequately represent changes in solute concentration along both the rising and falling limbs of the break through curve (BTC) (Figure 2).
1. Upon arrival of the solution (detected via an increase in conductivity), collect samples in 125 ml bottles throughout the BTC by holding a 125 ml bottle into the main flow of water at the sampling point. Quickly rinse the bottle with stream water and discard rinse downstream and then take sample. Cap sample and place into cooler.
2. Record the time (hr:min:sec) and conductivity of each sample taken along the BTC into a field book (Table 1).
3. Collect samples based on time (e.g. 1 min intervals) or based on the rate at which conductivity changes. For example, if conductivity is changing quickly, sample every 30-60 sec until changes in conductivity slow, at which time samples can be taken every 5-10 min. For intervals based on conductivity, take samples every 15-30 units depending on the rate at which conductivity is changing.
4. Sample until conductivity returns to background or within 5 µS/cm of background conditions. Intervals of sample collection can be adjusted during the experiment as long as the BTC is well represented in the grab samples.

Bottle #	Specific Conductance	Time	Notes
1		hr:min:sec	e.g. background (downstream)
2			e.g. background (downstream)
3
4
5			e.g. sample at peak conductance
.
.
.
Highest Bottle #

Table 1PField book: Example Page from Lab Book and Required Information

Sample Filtering
Note: Filtering of samples can occur either in the field or upon returning to the laboratory.
1. Filter samples from the rising limb in order of ascending specific conductivity until the peak in specific conductivity. Wait for the experiment to be over and filter samples from the falling limb in ascending order of specific conductivity (i.e. start with the last sample and work backwards toward peak specific conductivity).
  Note: This order of samples minimizes cross contamination between samples and allows for the same filter, syringe, and filter holder to be used as long as the filter, syringe and filter holder are appropriately rinsed in between each sample (see steps 5.3.2-5.3.4).
2. Remove plunger from a 60 ml syringe and then close stop-cock. Pour ~10 ml of sample into syringe and return plunger to syringe. Shake syringe so that sample rinses internal walls of syringe. Attached syringe to filter-holder and open stop-cock. Push sample through filter-holder and discard rinse.
3. Remove plunger and close stop-cock. Pour ~30 ml of sample into syringe and return plunger to syringe. Open stock-cock and expel ~10 ml through filter-holder and into 60 ml sampling bottle. Cap the bottle, swirl with filtrate and discard. Repeat this step for a total of 3 rinses. This will ensure any impurities have been removed from the 60 ml sample bottle and that the walls are coated with sample.
4. Remove plunger and close stop-cock. Pour ~60 ml of sample into syringe and return plunger to syringe. Push the sample through the filter holder and into the 60 ml sample bottle. Fill bottles up to the shoulder to prevent cracking of bottles when frozen. Cap bottle and place into cooler.
5. Repeat steps 5.3.2-5.3.4 for all remaining samples. Change filter between rising and falling limb samples to minimize contamination.
6. Transport samples back to the laboratory on the same day and on ice.

6. Preparation for Laboratory Analysis

If filtering of samples is to occur in the laboratory, follow protocol as outlined in section 5.3.1. Filter samples from both the ascending and descending limbs of the BTC in order of increasing conductivity. Change the filter between rising limb and falling limb samples.
Freeze filtered samples at -20 °C until analysis.
Ensure that analytical facilities are equipped to handle highly concentrated samples.
Note: Some laboratories are not equipped to run highly concentrated samples and thus care should be taken. Incorporate prepared standards that capture that higher end of expected solute concentrations. High concentration standards will help to ensure a standard curve that captures the expected range of manipulated solute concentrations.
Analyze samples from low to high conductivity on all analytical instruments. Ordering samples from low to high specific conductance prevents contamination of low salt/nutrient samples by high salt/nutrient samples. This means samples from the rising and falling limbs will be mixed with respect to sequence.
1. Analyze samples for total dissolved organic carbon, total dissolved nitrogen, nitrate and ammonium, although the exact combination of solute analysis will be a function of the research question (see Wymore et al.¹⁰ for example).

7. Data Analysis

Analyze the data using simple linear regression. The independent variable is the concentrations of the added nutrient and the dependent variable is DOM concentration either as DOC or DON. Each point on the figure represents one grab sample from the breakthrough curve and that sample's nutrient and DOC/DON concentration.

Representative Results

Figure 3: Example Results from Nitrate (NO₃^–) Additions with Dissolved Organic Nitrogen (DON) as the Response Variable. Analyses are linear regressions. Asterisks represent statistical significance at α = 0.05. Note the dynamic range in NO₃^– concentration that was achieved with the nutrient pulse method. Different panels represent different experiments across months and sites. Site acronyms refer to the three experimental streams¹⁰. Positive correlations are interpreted to reflect DON's role as a nutrient source while negative correlations are interpreted to reflect DON's role as an energy source. Experiments that resulted in no significant relationship are interpreted as either to reflect a non-responsive DON pool (i.e. highly recalcitrant) or that nutrient-based processes and energy-based process are off-setting. Please see Wymore et al.¹⁰ for additional discussion of results. Please click here to view a larger version of this figure.

Figure 4: Example Results from Nitrate (NO₃^–) Additions with Dissolved Organic Carbon (DOC) as the Response Variable. Analyses are linear regressions. Asterisks represent statistical significance at α = 0.05. Different panels represent different experiments across months and sites. Site acronyms refer to the three experimental streams¹⁰. Across the majority of experiments no significant changes in the ambient DOC pool were observed. Negative results can be revealing about coupled biogeochemical processes. Please see Wymore et al.¹⁰ for additional discussion of results. Please click here to view a larger version of this figure.

Through the direct in situ manipulation of NO₃^–, we were able to indirectly alter concentrations of the DOM pool providing insight into the biogeochemical controls on the ambient DOM pool. Figure 3 shows results from a study that examined the interaction between NO₃^– and DON¹⁰. Although the exact magnitude of solute increase varied across experiments (due to variation in background solute concentration) sufficiently large gradients of NO₃^– were created via the nutrient addition approach. From this set of experiments, across three watersheds in New Hampshire, USA, we are able to make inferences about the ecological role of DON in headwater streams. As an organic nutrient, DON may serve as either an energy source (carbon) or as a nitrogen source. In these low NO₃^– streams, we interpreted the increase in DON concentration to reflect its utilization as a nutrient source. By providing the microbial communities with a highly available form of N as NO₃^–, the community shifted from DON to this newly available form. This has previously been referred to as the DON release hypothesis¹⁵. In contrast, the negative correlations we observed during these nitrate manipulations are interpreted to reflect DON utilization as an energy source. This heterotrophic process has been termed the passive-carbon vehicle hypothesis^1,15. The highly variable response of DON throughout the growing season suggests strong seasonality in how DON responds to added nutrients. These data provide some of the first field-based experimental results regarding the ecological role that DON serves within stream ecosystems.

Negative results from these ecosystem manipulations are also revealing with respect to controls on biogeochemical processes. For example, Figure 4 shows no measurable response in the ambient DOC pool to the addition of NO₃^–. This suggests that the ambient pool of DOC is highly recalcitrant (i.e. not bioreactive). When nutrient pulses are repeatedly performed over the growing season for example, we can make inferences and conclusions about how and when the different fractions of the DOM pool are used by aquatic microbial communities. Through these manipulative ecosystem-scale experiments we were able to discern interactions between certain fractions of the DOM pool across a dynamic range of the added nutrient. These results in particular suggest that the N-rich fraction and C-rich fraction of the DOM pool cycle independently and may have their own unique set of ecological and biogeochemical controls^16,17. By using this nutrient addition method we have been able to provide manipulative field-based data which provides strong evidence and support to patterns of DON lability that had only previously been observed in laboratory incubations^18,19.

Discussion

The objective of the nutrient pulse method, as presented here, is to characterize and quantify the response of the highly diverse pool of ambient stream water DOM across a dynamic range of an added inorganic nutrient. If the added solute sufficiently increases the concentration of the reactive solute, a large inferential space can be created to understand how the biogeochemical cycling of DOM is linked to nutrient concentrations. This nutrient pulse approach is ideal as it involves none of the machinery associated with plateau-style addition (e.g. peristaltic pump) and does not involve expensive isotopic techniques. These manipulations are easily reproducible and multiple experiments can be conducted during a single day. We do recommend however, that if replicating experiments on the same day within a single stream reach, that additions are separated by several hours to allow for sufficient flushing of residual solutes.

In these ecosystem manipulations we are able to measure changes in the concentration of the ambient pool of DOM in response to the addition of nutrients. However, with this approach it is not possible to comment on which component of the DOM pool actually decreased or increased beyond changes in the concentration of DON and DOC. We cannot discern if it is a certain form of DON for example, that is preferentially consumed with the addition of NO₃^–. Changes could be due to a highly abundant and available forms of DON (e.g. amino acids) that were altered enough to change the overall concentration. However, this field-based approach could be easily paired with high-resolution analytical chemistry methods (e.g. fluorescence spectroscopy, Fourier transform ion cyclotron resonance mass spectroscopy) to determine what components or classes of molecules are directly responding to the experimental manipulation.

In addition to DOM chemistry, other biological and environmental factors may influence the response of DOM to the added nutrient. To understand this multifactor interaction other field data can be collected to examine other important variables. Temporal changes in the direction of the DON response to nitrate (Figure 3A-3F) may reflect autotrophic vs. heterotrophic dominated processes. For example, the positive relationship in Figure 3A, may reflect the activity of autotrophic organisms. It is likely that in May there is still adequate photosynthetically active radiation reaching the stream (prior to riparian canopy closure) and the observed pattern reflects these organisms shifting from DON to NO₃^– as their source of nitrogen, which results in an increase in DON concentration. The negative relationship observed later in the season (e.g. Figure 3E), likely represents the activity of heterotrophic microorganisms who are mining DON for its energy content. To test this type of biologically-based hypothesis, future research could incorporate concurrent measurements of autotrophic standing stock, microbial activity levels or enzymes concentrations, for example. Examining DOM-nitrate interactions across other environmental gradients, including dissolved oxygen and temperature, could help to elucidate the role of other physio-chemical parameters in driving the coupled biogeochemistry of DOM and nitrate.

The selection of low NO₃^– streams is essential for the success of these experiments and to retain the ability to measure changes in the DON pool. Studies examining the interaction between NO₃^– and DON for example, should occur in streams where NO₃^– makes up less than 50% of the TDN pool. The precision of measuring DON via subtraction is greatly reduced when NO₃^–contributes too large a fraction of the TDN pool since there is a multiplicative error term surrounding DON measurements that results from the analysis of TDN, NO₃^– and NH₄⁺. Such sub-optimal conditions can result in negative DON concentrations. Thus this technique may be limited in systems which are heavily impaired by NO₃^– such as estuaries.

Although larger streams and rivers present their own set of challenges, this method may be applicable to higher-order systems. For example, Tank et al.⁵ performed a nutrient pulse experiment in the 7^th-order Upper Snake River in Wyoming to examine the uptake kinetics of dissolved inorganic N. There may be ways to perform similar experiments in either lakes, soils or groundwater. However, such experiments are difficult due to the challenges associated with exposing a system to a gradient of nutrient concentrations or containing experimental units in ways that minimize disruption and experimental artefacts. This is one of the advantages of using stream ecosystems for these types of manipulative experiments. Nonetheless, the development of similar methods for other ecosystems, especially systems impaired by excessive N loading (e.g. estuaries), could have important management implications as we begin to understand the ways in which different forms of N drive eutrophication and toxic algal blooms in coastal waters.

Declarações

The authors have nothing to disclose.

Acknowledgements

The authors acknowledge the Water Quality Analysis Laboratory at the University of New Hampshire for assistance with sample analysis. The authors also thank two anonymous reviewers whose comments have helped to improve the manuscript. This work is funded by the National Science Foundation (DEB-1556603). Partial funding was also provided by the EPSCoR Ecosystems and Society Project (NSF EPS-1101245), New Hampshire Agricultural Experiment Station (Scientific Contribution #2662, USDA National Institute of Food and Agriculture (McIntire-Stennis) Project (1006760), the University of New Hampshire Graduate School, and the New Hampshire Water Resources Research Center.

Materials

Sodium Nitrate	Any	Any
Sodium Chloride	Any	Any	Store purchased table salt can be used as well, however, it does contain trace levels of impurities
Whatman GFF glass-fiber filters	Any	Any
BD Filtering Syringe	Any	Any
EMD Millipore Swinnex Filter Holders	Any	Any
Syringe stop-cock	Any	Any
YSI Multi-parameter probe	Yellow Springs International	556-01
Wide mouth HDPE 125 ml bottles	Any	Any
60 ml HDPE bottles	Any	Any
20 L bucket	Any	Any
Field measuring tape	Any	Any
Lab labeling tape	Any	Any
Stir stick	Any	Any
Cooler	Any	Any
Sharpie pen	Any	Any
Field notebook	Any	Any
Tweezers	Any	Any
Zip-lock bags	Any	Any

Referências

Brookshire, E. N. J., Valett, H. M., Thomas, S. A., Webster, J. R. Atmospheric N deposition increases organic N loss from temperate forests. Ecosystems. 10 (2), 252-262 (2007).
Bernhardt, E. S., McDowell, W. H. Twenty years apart: Comparisons of DOM uptake during leaf leachate releases to Hubbard Brook Valley streams in 1979 and 2000. J Geophys Res. 113, G03032 (2008).
Taylor, P. G., Townsend, A. R. Stoichiometric control of organic carbon-nitrate relationships from soils to sea. Nature. 464, 1178-1181 (2010).
Mulholland, P. J., et al. Stream denitrification across biomes and its response to anthropogenic nitrate loading. Nature. 452, 202-205 (2008).
Tank, J. L., Rosi-Marshall, E. J., Baker, M. A., Hall, R. O. Are rivers just big streams? A pulse method to quantify nitrogen demand in a large river. Ecology. 89 (10), 2935-2945 (2008).
Covino, T. P., McGlynn, B. L., McNamara, R. A. Tracer additions for spiraling curve characterization (TASCC): quantifying stream nutrient uptake kinetics from ambient to saturation. Limnol Oceanogr. 8, 484-498 (2010).
Johnson, L. T., et al. Quantifying the production of dissolved organic nitrogen in headwater streams using 15 N tracer additions. Limnol Oceanogr. 58 (4), 1271-1285 (2013).
Rosemond, A. D., et al. Experimental nutrient additions accelerate terrestrial carbon loss from stream ecosystems. Science. 347 (6226), 1142-1145 (2015).
Diemer, L. A., McDowell, W. H., Wymore, A. S., Prokushkin, A. S. Nutrient uptake along a fire gradient in boreal streams of Central Siberia. Freshwater Sci. 34 (4), 1443-1456 (2015).
Wymore, A. S., Rodríguez-Cardona, B., McDowell, W. H. Direct response of dissolved organic nitrogen to nitrate availability in headwater streams. Biogeochemistry. 126 (1), 1-10 (2015).
Stream Solute Workshop. Concepts and methods for assessing solute dynamics in stream ecosystems. J N Am Benthol Soc. 9 (2), 95-119 (1990).
Kilpatrick, F. A., Cobb, E. D. . Measurement of discharge using tracers: U.S Geological Survey Techniques of Water-Resources Investigations. , (1985).
Rodríguez-Cardona, B., Wymore, A. S., McDowell, W. H. DOC: NO3- and NO3- uptake in forested headwater streams. J Geophys Res – Biogeo. 121, (2016).
Kilpatrick, F. A., Wilson, J. F. Book 3 Chapter A9, Measurement of time of travel in streams by dye tracing. Techniques of Water-Resources Investigations of the United States Geological Survey. , (1989).
Lutz, B. D., Bernhardt, E. S., Roberts, B. J., Mulholland, P. J. Examining the coupling of carbon and nitrogen cycles in Appalachian streams: the role of dissolved organic nitrogen. Ecology. 92 (3), 720-732 (2011).
Michalzik, B., Matzner, E. Dynamics of dissolved organic nitrogen and carbon in a Central European Norway spruce ecosystem. Eur J Soil Sci. 50 (4), 579-590 (1990).
Solinger, S., Kalbitz, K., Matzner, E. Controls on the dynamics of dissolved organic carbon and nitrogen in a Central European deciduous forest. Biogeochemistry. 55 (3), 327-349 (2001).
Kaushal, S. S., Lewis, W. M. Patterns in chemical fractionation of organic nitrogen in Rocky Mountain streams. Ecosystems. 6 (5), 483-492 (2003).
Kaushal, S. S., Lewis, W. M. Fate and transport of organic nitrogen in minimally disturbed montane streams of Colorado, USA. Biogeochemistry. 74 (3), 303-321 (2005).

Play Video

PDF

DOI

DOWNLOAD MATERIALS LIST

Citar este artigo

Wymore, A. S., Rodríguez-Cardona, B., McDowell, W. H. Understanding Dissolved Organic Matter Biogeochemistry Through In Situ Nutrient Manipulations in Stream Ecosystems. J. Vis. Exp. (116), e54704, doi:10.3791/54704 (2016).