Natural Source Zone Depletion (NSZD)

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Natural source zone depletion (NSZD) is a term used to describe the collective, naturally occurring processes of dissolution, volatilization, and biodegradation that result in mass losses of light non-aqueous phase liquid (LNAPL) petroleum hydrocarbon constituents from the subsurface. NSZD is coming to the forefront of decision making at petroleum hydrocarbon remediation sites because much higher source attenuation rates are now being measured compared to previous rates based on incomplete conceptual models[1][2][3]. NSZD processes occur at most petroleum release sites and quantifying NSZD rates is an important part of an overall site remediation strategy.

Related Article(s):


CONTRIBUTOR(S): Tom Palaia and Jeff Fitzgibbons


Key Resource(s):

Introduction

After a release into the environment, petroleum hydrocarbon constituents in LNAPL undergo various different degradation processes including dissolution, volatilization, and biodegradation[6][7][8][9]. Natural Source Zone Depletion (NSZD) is a term used to describe these collective processes that result in mass losses of LNAPL petroleum hydrocarbon constituents from the subsurface. NSZD processes occur naturally within LNAPL-impacted zones in the subsurface. These processes physically degrade the LNAPL by mass transfer of chemical components to the aqueous and gaseous phases where they are biologically broken down via anaerobic and aerobic biodegradation.

Traditional methods of NSZD monitoring have focused on the groundwater transport of the solubilized LNAPL constituents and aqueous phase biodegradation that occurs through various terminal electron acceptor processes. Aerobic respiration, denitrification, sulfate reduction, iron and manganese reduction, and methanogenesis each support hydrocarbon degradation as the supply of each electron acceptor (e.g., dissolved oxygen, nitrate, sulfate), oxidation-reduction state, and the microbiological conditions allow. These processes manifest themselves as decreases in dissolved electron acceptor concentrations and production of soluble byproducts such as ferrous iron, dissolved methane (CH4), and carbon dioxide (CO2). Through stoichiometric conversion of the mass of electron acceptor loss and byproduct formation, the soluble or aqueous contribution to NSZD can be estimated[10][11][8].

Palaia-Article 1-Figure 1.PNG

Understanding of the gaseous expression of NSZD processes has recently improved via emerging research[12][9][13][2]. A large advance occurred with respect to the measurement of the significant amount of gases that can be produced because of anaerobic petroleum hydrocarbon biodegradation processes, predominantly methanogenesis[12]. Within the highly reduced saturated zone and overlying capillary fringe, methanogenesis occurs and generates CH4 and CO2. Because of the relatively low solubility of CH4, it is subsequently transported up to the vadose zone along with smaller amounts of CO2 and volatile organic compounds (VOCs). Within the vadose zone, LNAPL, CH4, and volatile hydrocarbons are anaerobically and aerobically biodegraded removing CH4 and oxygen (O2) from the soil gas and adding CO2. The biological oxidation of methane in the vadose zone is an exothermic process which releases heat to the surroundings[14][15]. We can conceptualize these vapor transport-related NSZD processes that are occurring at petroleum release sites as shown in Figure 1. In response to this improved understanding of NSZD, new monitoring methods have evolved to use stoichiometric conversion of the gaseous signatures left by NSZD in soil vapor or groundwater, as well as other lines of evidence such as thermal monitoring.

NSZD processes occurring within the subsurface manifest themselves as physical and chemical changes to both the aqueous and gaseous phases. The NSZD rate can be quantified by incorporating their petroleum hydrocarbon stoichiometric mass loss equivalents[5]. The methods and procedures to do this are described below.

Significance

Quantifying site-specific NSZD rates is important for various reasons. First, NSZD forms an important part of the LNAPL conceptual site model (LCSM), the written and/or illustrative representation of the physical, chemical, and biological processes that control the transport, migration, and actual/potential impacts of contamination. Within the LCSM, NSZD establishes a remediation baseline and supports interpretation of contaminant delineation and concentration trends. NSZD measurements can be used to:

  • Refine the LCSM with quantification of LNAPL loss rates
  • Delineate the LNAPL footprint using vadose zone indicators of biodegradation
  • Support estimates of remedial timeframes
  • Assess LNAPL stability through application of a mass balance of losses and measured mobile LNAPL flux[16]

Measured NSZD rates can also form the basis for remediation technology selection, design, and optimization. For example:

  • Comparing LNAPL mass removal rates from NSZD to other future potential remedial actions
  • Supporting a cost/benefit analysis of future remediation by evaluating the value of additional remediation compared to NSZD
  • Evaluating remedial progress via periodic NSZD measurements during static, re-equilibration periods in areas of residual hydrocarbons during an active remediation program
  • Using NSZD rates as an endpoint for active remediation

Throughout the remediation life cycle, measured NSZD rates can be used for a variety of decision-making purposes, ranging from technology selection to system shutdown or site closure.

Measuring the NSZD Aqueous Expression

NSZD is quantified by assuming the petroleum hydrocarbon stoichiometric equivalent of biodegradation expresses itself by changes in both the aqueous (soluble) and gaseous (vapor) phases[5]. This section covers the aqueous component. Within the saturated zone, aerobic respiration, denitrification, sulfate reduction, iron and manganese reduction, and methanogenesis each support hydrocarbon degradation and LNAPL mass loss.

Table 1. Terminal electron accepting processes associated with the aqueous expression of NSZD (for decane, excerpt from Johnson et al. (2006)[9]).
Figure 2a. IsoFlask Sampling Protocol.
Figure 2b. IsoFlask dissolved gas sampling results for LNAPL-impacted (triangles) and background (circle) locations.

For example, nitrate, iron, sulfate, and manganese reduction are some of the representative reactions for each process (Table 1). These processes manifest themselves as decreases in dissolved electron acceptor concentrations and production of soluble byproducts such as ferrous iron and dissolved CH4 and CO2. The soluble or aqueous contribution to NSZD can be estimated through stoichiometric conversion of the mass of electron acceptor loss and byproduct formation[10][8]. Because these estimates can be made using conventional groundwater sampling and analytical methods, the saturated zone component of NSZD is relatively well understood, and well-established procedures have been in place for over 20 years to monitor the NSZD process. However, conventional sampling programs often use open-system sample collection methods in which the sample is in direct contact with the atmosphere (e.g., direct fill and inverted VOA sampling methods). If the groundwater has elevated dissolved gas concentrations, some fraction of those gases may be lost to the atmosphere during sample collection.

The IsoFlask methodology (Figure 2a) uses a closed system where both dissolved and effervescing gases are captured and measured in the laboratory, which may provide more accurate results of dissolved gas analysis[17]. As seen in Figure 2b, results from an NSZD site evaluation indicated higher methane and carbon dioxide dissolved gas concentrations in the LNAPL-impacted locations as compared to the clean, background location.

The aqueous contribution to NSZD, historically known as the microbiological natural attenuation rate or assimilative capacity, is typically calculated using a mass budgeting approach[8]. The mass budgeting approach estimates dissolved hydrocarbon constituent losses within the saturated zone based on changes in the aforementioned electron acceptors and byproducts across transects through the hydrocarbon plume that spans upgradient and downgradient areas. Changes in concentrations for each process are stoichiometrically converted to hydrocarbon losses using the coefficients in Table 1. Groundwater models such as BIOSCREEN combine this mass budgeting approach with an advection dispersion model[11].

Measuring the NSZD Gaseous Expression

Current NSZD practice is to evaluate the petroleum hydrocarbon stoichiometric equivalent of biodegradation in both the aqueous phase and gaseous (vapor) phase[5]. This section covers the gaseous component.

At one site, the gaseous expression of NSZD has been shown to account for >70% of the hydrocarbon biodegradation that occurs in the subsurface[18][19]. Three methods to monitor the vapor phase-related portion of NSZD are currently available and widely used. These are the gradient, passive flux trap, and dynamic closed chamber (DCC) methods elaborated on below. Method choice for a particular project is a site-specific judgment based on data quality, monitoring objectives, and site conditions.

New NSZD monitoring methods continue to emerge, including an approach that uses thermal gradients[20]<[21]. Due to their limited applications, however, these emerging methods are not discussed herein.

Gradient Method

Figure 2c. Schematic of a typical gradient method monitoring setup (excerpt from Johnson et al. (2006)[9]).

The gradient method uses O2 or CO2 concentration profiles in soil gas and select subsurface properties (e.g., effective soil gas diffusion coefficients) to estimate the flux of gases through the vadose zone using Fick’s first law[22]. The change in concentration of these gases with depth within un-impacted soil above the petroleum hydrocarbons is used as a basis for estimating the flux:

Palaia-Article 1-Equation 1.PNG

where Palaia-Article 1-Fraction 1.1.PNG is the effective diffusion coefficient of the gas of interest in the vadose zone soils, and Palaia-Article 1-Fraction 1.2.PNG is the vertical concentration gradient of the gas being used to estimate NSZD rates. The gas flux is then stoichiometrically converted to an NSZD rate. This gradient method was the first published method to estimate NSZD[9].

A typical gradient method NSZD monitoring setup primarily includes a nested set of soil vapor probes installed above the LNAPL-impacted soils (Figure 2c). Soil gas samples are collected from the probes using industry-standard procedures and analyzed using a field landfill gas meter (e.g., LANDTEC GEM2000).

Two key elements to implementing the gradient method include selection of the depth intervals for calculating dC/dz and estimation of Dveff. The gradient can be estimated in a linear manner, using two points, and include the ground surface and atmospheric conditions as the upper control point. The lower control point is ideally situated immediately above the hydrocarbon oxidation zone, where oxygen is depleted and methane is absent. While literature values of Dveff could be used in a screening application of the gradient method, it is best to either empirically estimate the parameter using Millington and Quirk (1961)[23] or measure it directly[24].

Passive Flux Trap

Figure 3a. Schematic (left) and photo (right) of a passive CO2 Flux Trap (Used with permission from E-Flux, LLC. Soil Gas Flux)
Figure 3b. How Carbon Traps Work.

A passive flux trap is a flow-through, static chamber fitted with a chemical trap that has historically been used to measure soil-surface CO2 efflux[25]. The passive flux trap method was recently adapted for NSZD monitoring[2] and subsequently commercialized and further refined by E-Flux, LLC in Fort Collins, Colorado. The E-Flux CO2 trap employs the use of a dual-sorbent design to collect CO2 leaving the subsurface (Figure 3a). Although other configurations are possible, the trap is typcally installed in the shallow ground surface (i.e., 1–3 inches deep) and left in place for a 1–2 week timeframe. Over this time, CO2 derived from LNAPL degradation (i.e., fossil fuel-derived CO2) migrating upward from the subsurface to the atmosphere is collected inside the receiver pipe by a bottom caustic sorbent element. An upper sorbent element captures atmospheric CO2 (i.e., modern CO2) to avoid cross-contamination of the lower sorbent element, which is solely used for the NSZD estimate. The trap is deployed for a period of time that does not allow for either the top or bottom elements to become saturated with CO2. After the deployment period, the trap is retrieved and shipped to a laboratory for analysis of CO2. The CO2 efflux is estimated by dividing the trip blank-corrected mass of CO2 sorbed on the lower element by the deployment duration and the cross sectional area of the received pipe. Finally, a 14C correction is employed to separate the flux of modern CO2 flux (such as from decay of vegetation) from the “ancient” CO2 flux (from the biodegradation of petroleum products). For a more detailed explanation see the video “How Carbon Traps Work” (Figure 3b).

Dynamic Closed Chamber (DCC) Method

Palaia-Article 1-Figure 4.PNG

A DCC system is an active, specially adapted, direct measurement approach to estimate soil gas efflux at the ground surface. It pumps a small, closed loop circulation of air between a chamber set on a soil collar shallowly embedded in the ground surface and an external non-destructive gas analyzer that monitors the increase in CO2 concentration. To minimize errors associated with pressure differential inside and outside of the chamber, it is fitted with an engineered vent. DCC has been demonstrated to be a consistent efflux measurement method and used as reference for comparison to others[26]. The DCC has been used primarily for ecological carbon monitoring purposes and was recently adapted for NSZD monitoring[13]. Figure 4 shows an example DCC system, the LI-COR® 8100A automated soil flux system (LI-COR® BioSciences, Inc., Lincoln, Nebraska), and its typical setup for NSZD monitoring.

Using an internal pump, the DCC system circulates vapor that has accumulated within the chamber through a closed loop. Through continuous circulation and in-line measurement of the CO2 concentration by the non-destructive infrared gas analyzer (IRGA), the temporal increase in CO2 is recorded. The CO2 efflux is estimated using a curve fitting routine on the time series CO2 concentration data and dividing the results by the cross sectional area of the soil collar. The DCC collects rapid CO2 efflux measurements over a period of ~ 2 minutes. A series of multiple measurements are typically recorded during each field event. A long-term DCC system is also commercially available for automated, repeated measurement programs[27][28].

Gaseous Flux Background Correction

The gaseous expression of NSZD is complicated by concurrent, non-petroleum related processes that also consume O2 and create CO2[29]. These “background” processes include contributions from plant roots and microbes present in surficial and deeper soils containing natural organic matter. Therefore, correction is needed to subtract these effects prior to using the data from the gradient method and the two CO2 efflux methods (i.e., trap and DCC) for NSZD estimates. Options to eliminate the gaseous contributions of non-petroleum related sources include:

  • Install measurement locations in a nearby uncontaminated setting with similar surface and subsurface conditions. Calculation of NSZD rates using this approach involves subtracting the gaseous flux measured at the background location from the total flux at each survey location atop the LNAPL footprint.
  • Use radiocarbon-14 (14C) analysis on the CO2 collected from either the soil gas probes (gradient method) or the passive flux traps. The use of 14C provides an alternative, more accurate means to isolate the NSZD-derived CO2 efflux without the need to monitor outside areas. Background corrections using 14C are well documented[30][2].

Converting Gaseous Flux to an NSZD Rate

Palaia-Article 1-Figure 5.PNG

After elimination of gaseous effects due to non-petroleum processes, the corrected flux results can then be used to estimate a NSZD rate. A NSZD rate is typically expressed as a hydrocarbon degradation rate per unit area in a unit such as grams per square meter per day (g/m2/d). Using O2 or CO2 flux input, the NSZD rate is calculated by multiplying the background corrected gas flux, typically expressed as micromoles per square meter per second (mmol/m2/s), by the molar ratio of hydrocarbon degraded in a representative mineralization reaction as shown for octane:

Palaia-Article 1-Equation 2.PNG

Stoichiometry is used to determine a mass-based NSZD rate from gaseous flux data. The mass-based unit can be converted to a volume-based unit, for example gallons per square foot per day (gal/ft2/day), using the density of the predominant hydrocarbon at the site. If enough representative measurements are made over time to account for seasonal and/or hydrogeologic variability, for example, then the NSZD rate can expressed using an annual value such as gallons per acre per year (gal/ac/yr).

If enough representative measurements are made across the lateral extent of the LNAPL footprint, then a site-wide estimate of NSZD can be made. Stated simply, a site-wide NSZD rate (in units of mass per time) can be estimated by multiplying a unit area NSZD rate by an estimated lateral area of the LNAPL source zone. If unit area NSZD rates have been estimated at multiple locations, each can be apportioned to a representative area and totaled to arrive at a site-wide value. Figure 5 shows an example of mapping of NSZD rates from multiple DCC measurements at a site from which the site-wide NSZD rate was estimated to be 500 gallons per year (gal/yr).

Measuring the NSZD Thermal Expression

Figure 6a. Conceptual Model of Thermal Monitoring[31].
Figure 6b. Thermal monitoring video.

Analogous to a compost pile which generates heat, microbial biodegradation of LNAPL is an exothermic process that results in heat being transferred to the surroundings. As seen in Figure 6, microbial reactions include: i) methane generation in an anaerobic zone (both above and below the water table); and ii) methane oxidation in the unsaturated zone by bacteria which releases heat[14][15]. For instance, subsurface temperatures in LNAPL-impacted locations have been found to be consistently higher than background areas, with increases ranging from 2-2.5 °C[20], and up to 2.7 °C [21].

Figure 7a. Thermocouples installed on drill rods.
Figure 7b. Conventional Dril Rig.
Figure 7c. Weatherproof surface equipment enclosure with solar power.

Field Installation

Figure 8a. Background-corrected temperatures by depth.
Figure 8b. Thermal NSZD Dashboard Graph from an LNAPL Location Indicating Fluctuating Heat Signal from Biodegradation over Time at 10 ft bgs[32].

For continuous, remote monitoring of temperature data, thermal monitoring stations can be installed with consist of[31]:

  • Vertical profile of thermocouples installed by conventional drilling rigs (Figures 7a and 7b).
  • Datalogger and wireless communication system powered by solar panel (Figure 7c).
  • Weather-proof enclosure for monitoring electronics.

Other studies have used probes or data loggers installed in existing groundwater monitoring wells[20], or temperature data loggers housed in water-filled PVC pipe[21].

Converting Temperature to an NSZD Rate

Subsurface temperature data from a background (i.e., clean, no LNAPL impacts and with similar geology and surface type) location is needed in order to subtract seasonal temperature effects from the LNAPL-impacted location. In cases where representative background temperature measurements may not be available at a site, it is possible to estimate background temperature using mathematical models[20] (Hillel XXXX).

Conversion of the background-corrected temperature data requires: i) evaluation of the heat flux; and ii) conversion to an NSZD rate using the heat of reaction[15].

Heat conduction in the subsurface can be quantified using Fourier’s Law for heat flux in the vertical direction (Figure 8a) as follows:

qh = ‐KT(ΔT/Δz)

where:

qh is the heat energy lost across a surface (J/m2),
KT is the thermal conductivity (J/m-K),
ΔT is the change in temperature (K), and
Δz (m) is the depth interval across which heat flux is calculated.

The total heat flux (sum of heat flux to ground surface and heat flux downward) is converted to an NSZD rate (in gallons LNAPL degraded per acre per year) using the heat of reaction of hydrocarbon biodegradation (Figure 8b). The approximate heat released during the complete mineralization of decane is 6,797 kJ/mol (Stockwell 2015).

Limitations and Challenges

NSZD is occurring at most petroleum release sites, however, site-specific conditions will drive the magnitude of rates. For example, the presence of a “typical” gaseous expression of NSZD (Fig. 1) is contingent upon the presence of LNAPL and free exchange of atmospheric oxygen with the subsurface. If the site contains predominantly impervious ground cover, then NSZD processes will deviate from that described herein and procedures to measure it must be adapted accordingly. Many other site conditions such as low permeability soil layers, perching water or wet vadose zones, shallow water tables, and cold climates can also affect NSZD processes and must also be taken into account during the design of any NSZD monitoring plan.

NSZD rates measured using the methods described above quantify total hydrocarbon mass loss and do not speciate loss or degradation rates of individual chemicals such as benzene or naphthalene from soil or LNAPL phases. Therefore, the use of NSZD data for assessment of remedial timeframe, if based on time to achieve chemical-specific cleanup criteria in groundwater, for example, is limited. Current research is focused on correlating NSZD rates to better established remediation metrics such as LNAPL transmissivity and chemical-specific degradation rates. For example, Ng et al. (2015)[33] developed a mass balance model that provides some insights on the contributions of various hydrocarbon constituent classes to the overall NSZD rate at a crude oil research site.

Thermal monitoring requires background correction, similar to methods that measure vadose zone gas transport. Proper placement of temperature transducers in LNAPL-impacted as well as background locations is necessary in order to avoid errors in interpretation of the temperature data. Background thermal monitors should be located in areas with no LNAPL impacts, but with similar geology and surface cover type (e.g., vegetation). Additionally, both LNAPL-impacted and background monitors should be placed in areas without any additional sources of subsurface heat (e.g., active pipelines).

Lastly, NSZD rates can be variable. They can fluctuate seasonally with change in ambient temperature which may induce cold/warm temperature cycles in the subsurface and also fluctuate with changes in surrounding water use (e.g., irrigation pumping). Additionally, each method has its own unique procedure and inherent assumptions, which make its measurement results difficult to compare with others.

Due to these limitations and challenges, NSZD monitoring must be performed with a firm understanding of the data objectives and use, and a sound LCSM.

Summary

NSZD is an important process that is occurring at most petroleum release sites. Measuring the rate of NSZD can be very helpful in implementing an effective remediation strategy at these sites. Several approaches to measuring and quantifying NSZD rates are now available. However, as with most environmental remediation techniques, it is equally important to be cognizant of and account for the limitations and challenges with the approach and its associated measurements.

References

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  31. ^ 31.0 31.1 Thermal NSZD, 2018. Thermal NSZD: Continuous Remote Monitoring of Natural Source Zone Depletion
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  33. ^ Ng, G.-H. C., B. A. Bekins, I. M. Cozzarelli, M. J. Baedecker, P. C. Bennett, R. T. Amos, Herkelrath, W. N., 2015. Reactive transport modeling of geochemical controls on secondary water quality impacts at a crude oil spill site near Bemidji, MN, Water Resoures Research., 51, 4156–4183. doi: 10.1002/2015WR016964

See Also

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