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Research Article Volume 123 | Issue 7 | July 2015

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Environ Health Perspect; DOI:10.1289/ehp.1408855

Understanding the Radioactive Ingrowth and Decay of Naturally Occurring Radioactive Materials in the Environment: An Analysis of Produced Fluids from the Marcellus Shale

Andrew W. Nelson,1,2 Eric S. Eitrheim,3 Andrew W. Knight,3 Dustin May,2 Marinea A. Mehrhoff,2 Robert Shannon,4 Robert Litman,5 William C. Burnett,6 Tori Z. Forbes,3 and Michael K. Schultz1,7,8

Author Affiliations open
1Interdisciplinary Human Toxicology Program, University of Iowa, Iowa City, Iowa, USA; 2University of Iowa State Hygienic Laboratory, Research Park, Coralville, Iowa, USA; 3Department of Chemistry, University of Iowa, Iowa City, Iowa, USA; 4Quality Radioanalytical Support, Grand Marais, Minnesota, USA; 5Radiochemistry Laboratory Basics, The Villages, Florida, USA; 6Department of Earth, Ocean and Atmospheric Science, Florida State University, Tallahassee, Florida, USA; 7Department of Radiology, and 8Department of Radiation Oncology, Free Radical and Radiation Biology Program, University of Iowa, Iowa City, Iowa, USA

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  • Background: The economic value of unconventional natural gas resources has stimulated rapid globalization of horizontal drilling and hydraulic fracturing. However, natural radioactivity found in the large volumes of “produced fluids” generated by these technologies is emerging as an international environmental health concern. Current assessments of the radioactivity concentration in liquid wastes focus on a single element—radium. However, the use of radium alone to predict radioactivity concentrations can greatly underestimate total levels.

    Objective: We investigated the contribution to radioactivity concentrations from naturally occurring radioactive materials (NORM), including uranium, thorium, actinium, radium, lead, bismuth, and polonium isotopes, to the total radioactivity of hydraulic fracturing wastes.

    Methods: For this study we used established methods and developed new methods designed to quantitate NORM of public health concern that may be enriched in complex brines from hydraulic fracturing wastes. Specifically, we examined the use of high-purity germanium gamma spectrometry and isotope dilution alpha spectrometry to quantitate NORM.

    Results: We observed that radium decay products were initially absent from produced fluids due to differences in solubility. However, in systems closed to the release of gaseous radon, our model predicted that decay products will begin to ingrow immediately and (under these closed-system conditions) can contribute to an increase in the total radioactivity for more than 100 years.

    Conclusions: Accurate predictions of radioactivity concentrations are critical for estimating doses to potentially exposed individuals and the surrounding environment. These predictions must include an understanding of the geochemistry, decay properties, and ingrowth kinetics of radium and its decay product radionuclides.

  • Citation: Nelson AW, Eitrheim ES, Knight AW, May D, Mehrhoff MA, Shannon R, Litman R, Burnett WC, Forbes TZ, Schultz MK. 2015. Understanding the radioactive ingrowth and decay of naturally occurring radioactive materials in the environment: an analysis of produced fluids from the Marcellus Shale. Environ Health Perspect 123:689–696; http://dx.doi.org/10.1289/ehp.1408855

    Address correspondence to M.K. Schultz, Radiology and Radiation Oncology, University of Iowa, ML B180 FRRB, 500 Newton Rd., Iowa City, IA 52242 USA. Telephone: (319) 335 8017. E-mail: michael-schultz@uiowa.edu

    We acknowledge the staff and faculty at the University of Iowa State Hygienic Laboratory (SHL) for assisting us in this research.

    Funding for these experiments was provided by the U.S. Nuclear Regulatory Commission (NRC-HQ-12-G-38-0041) and by Environmental Management Solutions (contract EMS FP 07-037-43). R.S. is employed by Quality Radioanalytical Support, and R.L. is employed by Radiochemistry Laboratory Basics.

    M.K.S. is a paid consultant for Speer Law Firm, PA, Kansas City, Missouri. The other authors declare they have no actual or potential competing financial interests.

    Received: 21 June 2014
    Accepted: 11 March 2015
    Advance Publication: 2 April 2015
    Final Publication: 1 July 2015

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Introduction

New unconventional drilling technologies (horizontal drilling combined with hydraulic fracturing, called “fracking”) are unlocking vast reserves of natural gas in the United States and around the world (Cueto-Felgueroso and Juanes 2013; U.S. Energy Information Administration 2014). The potential economic value of these reserves has stimulated a rapid globalization of the approach (Boyer et al. 2011). However, the pace of proliferation of these practices has raised concerns about the potential for unintended and undesirable environmental impacts (Finkel 2011; Goldstein et al. 2012; Howarth et al. 2011; Kerr 2010; Schmidt 2011; Thompson 2012). One key environmental issue associated with unconventional drilling and hydraulic fracturing is the management of water resources and liquid wastes (flowback and produced fluids) (Clark and Veil 2009; Kondash et al. 2014; Lutz et al. 2013; Vidic et al. 2013; Yang et al. 2013; Zhang et al. 2014). Of the environmental contaminants documented in hydraulic fracturing liquid wastes, naturally occurring radioactive materials (NORM) are of particular concern (Brown 2014; Kargbo et al. 2010; Vengosh et al. 2014).

Recent attention has focused on unintentional releases of radium (Ra) isotopes from wastewater treatment plants (Warner et al. 2013), which can arise from incomplete treatment of high ionic strength flowback and produced fluids (Gregory et al. 2011). For example, breakthrough of untreated fluids at a waste treatment facility in central Pennsylvania (northeastern United States) led to Ra contamination in stream sediments measured to be a factor of 200 greater in radioactivity concentration than local background levels (Warner et al. 2013). The magnitude of the Ra contamination at this site prompted the plant operator to proceed with remediation of contaminated sediments in the surface water system (Blacklick Creek) impacted by the discharges (Hunt 2014). Thus, NORM contamination of local environments, arising from improper treatment and disposal of produced fluids, could emerge as an unintended consequence of hydraulic fracturing. Although the potential for local populations and workers to experience unhealthy exposures to NORM contained in such wastes is controversial (Brown 2014), monitoring the radioactivity concentrations in these materials is critical to the development of effective waste management strategies and exposure assessments. However, few peer-reviewed reports are available that document levels of NORM in produced fluids. Of those available from the Marcellus Shale (the largest shale-gas formation in the United States), most report radioactivity concentrations of a single element—Ra (Barbot et al. 2013; Haluszczak et al. 2013; Nelson et al. 2014; Rowan et al. 2011).

The naturally occurring Ra isotopes of concern (226Ra and 228Ra) have been reported (in peer-reviewed literature) to exceed 670 Bq/L and 95 Bq/L, respectively, in produced fluids (Barbot et al. 2013; Haluszczak et al. 2013; Nelson et al. 2014; Rowan et al. 2011). However, little attention has been paid to other environmentally persistent alpha- and beta-emitting NORM such as uranium (U), thorium (Th), radon (Rn), bismuth (Bi), lead (Pb), and polonium (Po) isotopes (Figure 1). In reviewing a report of gross alpha levels in fluids from Marcellus Shale, we observed that reported Ra radioactivity concentrations were similar to maximum gross alpha levels (Barbot et al. 2013), indicating that Ra had been selectively extracted into the liquid wastes, while alpha-emitting daughters remained insoluble under the geochemical conditions of the fluid extraction process. Given that Ra decay products had likely existed in a steady-state radioactive equilibrium with Ra isotopes in the solid shale-formation matrix for millions of years prior to drilling activities, these observations prompted us to explore the radioactive equilibrium relationships of Ra decay products in produced fluids, particularly for the longer-lived alpha-emitters, 228Th (t1/2 = 1.91 years) and 210Po (t1/2 = 138 days) (half-lives were extracted from the NuDat 2 Database) [National Nuclear Data Center (NNDC) 2013].

Figure 1 - Schematic diagram of the radioactive decay of thorium and uranium.Figure 1 – Natural thorium and uranium decay chains. Half-lives and decay information were obtained from the NuDat 2 Database (NNDC 2013). Abbreviations: d, days; h, hours; m, minutes; s, seconds; y, years.

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As we reported previously, the chemical composition of fluids from the Marcellus Shale can interfere with the analysis of Ra isotopes by wet chemistry methods (Nelson et al. 2014). However, the physicochemical properties of select alpha-emitters (210Po, 228Th, and certain U isotopes) allow for chemical extraction and analysis by isotope dilution alpha spectrometry techniques. Thus, we developed a method to analyze alpha-emitting Po, Th, and U isotopes in produced fluids from the Marcellus Shale. Using this method (in systems closed to the release of gaseous radon), we found that estimates of total radioactivity in produced fluids based on Ra isotopes alone can underestimate the total radioactivity present due to the ingrowth of Ra decay-product radionuclides, a process that we demonstrate can be modeled using radioactive ingrowth equations (Bateman 1910). This model predicts that when produced fluids are sealed to the release of radon gas, the total radioactivity concentration of produced fluid can increase by a factor greater than five within the first 15 days following extraction due to the ingrowth of Ra decay products. Measurements of decay series radionuclides 210Po and 228Th in produced fluids from the Marcellus Shale presented here support these predictions. Thus, estimates of the radioactivity associated with hydraulic fracturing liquid wastes must include projections of ingrowth of decay product radionuclides in the natural uranium (238U) and thorium (232Th) decay series.

Methods

General. The State Hygienic Laboratory (SHL) at the University of Iowa is accredited by the U.S. National Environmental Laboratory Accreditation Program (NELAP). Standard operating procedures and quality assurance measures meet those established by NELAP. All chemical reagents used were ACS grade or higher. All radioactivity values were decay corrected to the reference date of 7 May 2013, 0800 hours (CST). All uncertainties, unless indicated, are standard uncertainties corresponding to one standard deviation of multiple measurements (Currie 1968).

Tracers and standards. All radioactive tracers were a) standard reference materials (SRMs) obtained from the U.S. National Institute of Standards and Technology (NIST), b) NIST-traceable certified reference materials (CRMs) obtained from Eckert & Ziegler Radioisotopes (E&Z) or Analytics, or c) SRMs obtained from the United Kingdom National Physical Laboratory (NPL) Management Ltd. The following sources were used: a 3-L liquid Marinelli geometry (E&Z 93474), 210Pb (E&Z 94643), natU (E&Z CRM 92564), 232U (E&Z CRM 92403 or E&Z 7432; certified in equilibrium with 228Th), 230Th (NIST SRM 4342A or Analytics 67900-294), 209Po (NIST 4326 or E&Z CRM 92565), and multiline alpha-emitting sources (E&Z 91005, Analytics 59956-121, and Amersham AMR.43).

Sample description. A representative sample of produced fluids from northeastern Pennsylvania (Nelson et al. 2014) was used for all of the following experiments. A 200-L drum of Marcellus Shale produced fluids was received at the SHL on 7 May 2013. The sample originated from a well that was horizontally drilled to a depth of 2,100 m and fractured with approximately 35,000 m3 of hydraulic fracturing fluid in early 2012. Analysts at SHL characterized the elemental composition using standard techniques.

High purity germanium (HPGe) gamma spectrometry. HPGe gamma spectrometry of produced fluids was conducted as previously described (Nelson et al. 2014). Briefly, we calibrated our detector to a 3-L liquid Marinelli geometry (E&Z 93474) using standard practices. To calibrate for the low energy gamma emission of 210Pb, we counted a 3-L Marinelli beaker spiked with 210Pb of known activity (E&Z 94643). This spectrum was merged with the detector calibration using standard features available in ORTEC Gamma Vision (version 6.08, analysis engine Env32). Quality assurance and quality control (QA/QC) measures included weekly background counts, and linearity and efficiency checks collected three times per week. A 3-L sample was homogenized by heating with 51 g of Bacto Agar (BD 214010; Becton Dickinson) and allowed to cool in a 3-L Marinelli beaker. The sample was then counted for 17 hr on a 30% efficient ORTEC HPGe. Spectral analysis was performed using ORTEC Gamma Vision (Version 6.08) with a library of radionuclides created in GammaVision Library Editor according to the manufacturer’s recommendations. All emission energies, half-lives (except for that of 209Po), and their uncertainties were extracted from the NuDat 2 Database (NNDC 2013) and include evaluated nuclear data at the time of analysis. The sole exception was the half-life of 209Po, for which we chose to use 128.3 years (Collé et al. 2007).

Alpha-emitting radionuclides. Analysis of produced fluids for alpha-particle emitting radionuclides in the 238U and 232Th decay series (210Po, 228Th, 230Th, 234U, 235U, 238U) was conducted by preconcentration and isotope dilution alpha spectrometry. All results presented are from an unfiltered subsample (20 L, in a polypropylene carboy) drawn from the homogenized 200-L barrel. Following each subsampling, the barrel was hermetically sealed. The subsample pH was adjusted to 2 and held (approximately 48 hr) to allow iron-rich particulate to dissolve to a transparent, yellowish acidified solution. Preconcentration and matrix simplification were then conducted via coprecipitation of Po, Th, and U with endogenous iron (Fe) as the hydroxide [Fe(OH)3] and added manganese (Mn) for coprecipitation as manganese dioxide (MnO2), as previously described (Eichrom Technologies, LLC 2009; Harada et al. 1989). Preliminary experiments demonstrated exceedingly low concentrations of 230Th, allowing use of 230Th as a radiotracer to determine yields and concentration of 228Th. Following preconcentration and matrix simplification [via metal oxide/hydroxide co-precipitation; i.e., Fe(OH)3 and MnO2], Po, U, and Th were separated into radiochemically pure fractions via extraction chromatography.

MnO2 coprecipitations. Samples were spiked with 150–500 mBq of 209Po, 230Th, 232U, and natU. After appropriate tracers were added, MnO2 coprecipitations were performed, based on published methods (Burnett et al. 2012; Moore 1976; Nour et al. 2004). Potassium permanganate (15 or 30 mg) and bromocresol purple (1 mL, 0.1%) were added to acidified (pH < 2) produced fluid (0.5 L) in glass beakers. The sample was diluted 2-fold in distilled water (dH2O), covered with a watch glass, and boiled (1 hr). The pH was adjusted to 7–8, and the sample was boiled for 1 hr and cooled overnight. Following the cooling period, the supernatant was aspirated; the remaining slurry (~ 50 mL) was transferred to a plastic conical tube (50 mL) and centrifuged (10 min), and the supernatant was discarded. Beakers were washed twice (5 mL 6 M HCl; 1 mL 1 M ascorbic acid), each time transferring the wash liquid to the 50-mL centrifuge tube to dissolve the MnO2 pellets. Centrifuge tubes were then gently heated in a water bath to fully dissolve the pellet and clarify the solution.

Method 1: SR resin and silver (Ag) autodeposition separation of polonium. In some cases, Po isotopes were isolated following an Eichrom method (Eichrom Technologies LLC 2009). Briefly, samples were spiked with 209Po prior to MnO2 or Fe(OH)3 precipitation. Precipitates were dissolved (10 mL, 2 M HCl), reduced (1 mL, 1 M ascorbic acid), and gently heated in a water bath. Solutions were then loaded onto preconditioned Eichrom SR Resin (10 mL, 2 M HCl). Columns were rinsed (10 mL, 2 M HCl) to remove trace contaminants. Po was then eluted with two additions of acid [5 mL, 1 M nitric acid (HNO3); 15 mL, 0.1 M HNO3]. Eluent was wet ashed (0.5 M HCl) under low heat to remove HNO3. Samples were then dissolved (40 mL, 0.5 M HCl) and reduced (100 mg ascorbic acid). Po was then allowed to autodeposit overnight at 80°C onto Ag disks painted on one side with acid-resistant acrylic paint. Disks were then cleaned (~ 10 mL 0.5 M HCl, dH2O, ethanol, and acetone, in that order) and dried prior to alpha spectrometry.

Method 2: TRU-Ag-TEVA separation (final method). After MnO2 coprecipitation and solubilization, most samples (Table 1) were loaded onto preconditioned TRU cartridges (10 mL, 4 M HCl; Eichrom) to adhere Po, U, and Th (Horwitz et al. 1993). TRU resin (Eichrom) was washed three times (5 mL, 4 M HCl) before eluting Po, U, and Th (10 mL, 0.1 M ammonium bioxalate) into 150-mL glass beakers containing approximately 20 mL of 0.1 M HCl. The eluent was then reduced to prevent interferences from iron (0.5 mL, 20% wt/vol hydroxylamine·HCl; 0.1 mL, 1 M ascorbic acid) (Manickam et al. 2010). Samples were incubated (90°C) in a double boiler on a stir plate. A magnetic stir bar and a polished Ag disk (one side coated with acid-resistant acrylic spray-paint) were placed into the beaker. After 2.5 hr, disks were removed and washed (10 mL each 0.1 M HCl, H2O, ethanol, and acetone, in that order). The remaining solution was taken to dryness and resuspended (10 mL, 4 M HCl). U and Th were then separated on a TEVA cartridge (Eichrom) using a method developed in our laboratory (Knight et al. 2014). The solution of 4 M HCl containing U and Th was loaded onto a preconditioned TEVA column (10 mL, 4 M HCl). Th does not adhere to the column in these conditions. Therefore, Th was collected in the eluent of the load solution along with an additional column wash (10 mL, 4 M HCl). The column was then washed (25 mL, 4 M HCl) to remove trace Th before U was eluted (5 mL, 0.1 M HCl). Th was precipitated by a rare-earth hydroxide as follows: cerium (Ce; 30 μg), bromocresol purple (1 mL, 0.1%), and H2O2 (30 μL, 30%). The pH was adjusted to 7 with ammonium hydroxide and left undisturbed (30 min). U sources were prepared by a rare-earth fluoride precipitation by addition of Ce (50 μg), titanium trichloride (1 mL), and hydrofluoric acid (1 mL). U and Th samples were filtered on Eichrom Resolve Filters according to the manufacturer’s recommendation. For a workflow schematic, see Supplemental Material, Figure S1.

Table 1 - See HTML for full tableTable 1 – Activity, recovery, and separation method for select radioisotopes analyzed by alpha spectrometry of produced fluids.

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Method 3: TRU-TEVA for separation of U and Th. Reported activities of U in the produced fluids were determined using a method previously developed in our laboratory (Knight et al. 2014). This method differs only slightly from those described above. Briefly, the pellets were dissolved in HNO3 (10 mL, 2 M) and TRU resin was preconditioned and washed with HNO3 (10 mL, 2 M) in lieu of HCl. This method was investigated but abandoned, as it does not allow for analysis of 210Po.

Isotope dilution alpha spectrometry. All alpha sources were quantitated by standard isotope dilution techniques and counted in vacuum controlled α-spectrometers [Alpha Analyst (Canberra) or Alpha Ensemble (ORTEC)] as previously described (Knight et al. 2014). Briefly, source-to-detector distances were usually 10 mm, corresponding to a counting efficiency of approximately 18–30%. In some instances, the distance was increased to improve resolution. Radiochemical yields were determined by standard protocols using efficiencies calculated with a NIST traceable, multiline α-spectrometry standard source (E&Z 91005 or Analytics 59956-121). For all samples, thin films were used to prevent daughter recoil contamination of detectors (Inn et al. 2008). Sources were counted for 17–200 hr, as necessary. Standard isotope dilution techniques were used to calculate the activity and recoveries of added controls. In samples where 232U and 230Th were used, activity of 228Th introduced from the 232U tracer was subtracted using yield determinations for Th isotopes calculated by 230Th. QA/QC included blanks (no added tracers) and laboratory control spikes (LCS).

Radioactive ingrowth modeling. Radioactive ingrowth was modeled generally according to the Bateman equation (Bateman 1910) and solved in Microsoft Excel. The derivation and formatting of the Bateman equation was obtained from Choppin et al. (2002).

Results

Radiochemical disequilibria and ingrowth. Radiochemical yields for the final methodology were Po (81 ± 6%), U (63 ± 8%), and Th (85 ± 9%). The observed concentrations of natural U (238U, 235U, 234U), and Th isotopes (234Th, 232Th, and 230Th) were exceedingly low (< 5 mBq/L). These levels represented < 0.001% of the 226Ra radioactivity concentration (670 ± 26 Bq/L; 186 keV peak) in the sample of produced fluids described previously (Nelson et al. 2014). Similarly, we found that the radioactivity concentrations of Ra decay products, including 228Th, 214Pb, 214Bi, 212Pb, 210Pb, 210Po, and 208Tl, were initially near detection limits (Figure 2A–D, Tables 1 and 2; see Supplemental Material, “Expanded methods, Polonium-210 ingrowth”). In contrast, subsequent analysis of the same sample of produced fluids over time revealed an increase in the radioactivity concentration of decay products 210Po and 228Th, which are supported by 226Ra and 228Ra, respectively (Figure 1; Figure 2A,B). Importantly, the storage drum was hermetically sealed between subsamplings for analysis of radioactive decay products to prevent the release of gaseous radon. Notably, under these conditions, the observed increase in radioactivity concentration of 210Po and 228Th followed an established radioactive ingrowth model (Bateman equation), which describes the ingrowth of decay products following a separation (radioactive disequilibrium) of decay products from the parent radionuclide at time zero (t0). From these observations we developed a theoretical model for the geochemical partitioning of NORM in the Marcellus Shale formation, within the context of hydraulic fracturing and associated waste disposal activities (Figure 3). This model serves as a guide for predicting the partitioning and radioactive ingrowth/decay of NORM in the environment surrounding unconventional drilling and hydraulic fracturing operations, as well as in the waste treatment and disposal setting. Importantly, the ultimate fate and transport of NORM in the surface and subsurface environment is site dependent and depends on the potential for release of radon gas; thus, the assessment of the ultimate fate and transport of NORM must be examined on an individual site basis.

Figure 2 - A and B) Line graphs of radioactivity (y-axes) according to time (days, x-axes) for Pb210 and Po210, and for Th228 and Rz228, respectively. C) Graph of the Po alpha spectrum (y-axis = counts, x-axis = energy) for Po209 tracer and Po210.  D) Graph of the Th alpha spectrum (y-axis = counts, x-axis = energy) for Th230 tracer, Th228, and Th228 decay products.  E. Bar graph of mean activities (y-axis, with SD) for U238, U235, and U234 (x-axis). F) Graph of the U alpha spectrum (y-axis = counts, x-axis = energy) for U238, U235, U234, U232 tracer, and U232 tracer decay products.Figure 2 – Activity and alpha spectra of Po, Th, and U. (A) Theoretical Bateman model of 210Pb ingrowth (blue) and 210Po (red) given 226Ra levels and a system closed to emanation of gaseous radon in produced fluids sample with our empirical data (black squares; error bars subsumed within boxes). (B) Theoretical Bateman model of 228Th ingrowth (green) and 228Ra decay (blue) given 228Ra levels and a system closed to emanation of gaseous radon in produced fluids sample with our empirical data in black (error bars subsumed within boxes). (C) Representative Po alpha spectrum of 209Po tracer (orange) and 210Po (red). (D) Representative Th alpha spectrum of 230Th tracer (purple), 228Th (green), and 228Th decay products (black). 232Th was virtually undetectable by this method. (E) Activities of 238U (purple), 235U (black), and 234U (orange) in produced fluids; error bars represent one standard deviation of the determined activity of multiple counts (n = 3). (F) Representative U alpha spectrum of 238U (purple), 235U (not labeled), 234U (red), 232U tracer (blue), and 232U tracer decay products (228Th green; others black).

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Table 2 - See HTML for full tableTable 2 – HPGe gamma spectrometry of produced fluids.

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Figure 3 - Conceptual diagram showing NORM partitioning during different parts of the oil extraction process.Figure 3 – Theoretical model of NORM partitioning and associated waste in Marcellus Shale based on HPGe gamma spectrometry and alpha spectrometry of produced fluids. Solid arrows indicate a radioactive decay or series of radioactive decays. Dashed arrows indicate a physical or chemical partitioning process.

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Discussion

Modeling the partitioning NORM in Marcellus Shale. The partitioning U and Th decay series radionuclides in Marcellus Shale liquid wastes is a function of elemental geochemical behavior—linked with key biogeochemical features of the formation. Like many marine black shale formations, the Marcellus Shale is an ancient seabed that became enriched in U associated with organic matter (Carter et al. 2011; Kargbo et al. 2010; Swanson 1961). Produced fluids from the Marcellus Shale have characteristically high levels of salts, the origin of which has several explanations (Blauch et al. 2009). There are notably low levels of sulfate (SO42–) (Osborn and McIntosh 2010), likely due to microbial processes that produce sulfides (S2–) (Libes 1992). The ionic strength, reducing environment, and low abundance of SO42– alter the potential for NORM to solubilize in produced fluids. For example, low levels of SO42– and relatively high ionic strength enhance the solubility of Ra, whereas reducing conditions promote precipitation of geochemical species of reduced U, that is, U(IV). Radium decay product radionuclides, such as Pb and Po, are also much more particle reactive and less likely to be extracted through the unconventional drilling and hydraulic fracturing process than decay-series parent Ra isotopes. Thus, differences in the speciation of the elements in the natural decay series govern the likely concentration that will be observed in liquid wastes (as they emerge from depth), following an unconventional drilling and hydraulic fracturing event.

232Th Series partitioning. The parent and supporting isotope in the natural Th decay series, 232Th (t1/2 = 1.4 × 1010 years), is not expected to undergo oxidation/reduction reactions under natural conditions at depth in the formation, but is nonetheless particle reactive and insoluble in environmental waters and brines (Melson et al. 2012). Accordingly, we observed exceedingly low concentrations of 232Th in unfiltered Marcellus Shale produced fluids. However, the decay of 232Th produces highly soluble divalent alkaline earth 228Ra (t1/2 = 5.75 years), which has likely been in radioactive secular equilibrium (steady-state) with 232Th for many millions of years (Gonneea et al. 2008). As a result, produced fluids are enriched in 228Ra (relative to 232Th), which is highly soluble in the high-salt-content brines that describe produced fluids. 228Ra decays by beta emission to short-lived 228Ac (actinium-228; t1/2 = 6.15 hr), which likely forms insoluble complexes and quickly adsorbs to mineral surfaces at depth—and decays rapidly to form highly insoluble alpha-particle–emitting radionuclide 228Th (t1/2 = 1.91 years) (Hammond et al. 1988). Similar to other Th isotopes, 228Th is insoluble in interstitial fluids of shale formations, and its concentration is also low in produced fluids as they emerge from depth. Notably, the large difference in solubility between 228Ra and 228Th gives rise to a chronometer that has the potential to determine the time when fluids were extracted from the Marcellus Shale (for more information, see Supplemental Material, “Expanded methods, Thorium-228 ingrowth”). As 228Th ingrows at a rate related to its half-life, its decay product 224Ra (t1/2 = 3.63 days), rapidly ingrows to steady-state radioactive equilibrium. Rapid ingrowth of 224Ra is followed by a series of short-lived radioactive decay products that ultimately decay to stable 208Pb (Figure 1). Within this series of relatively short-lived decay products, gaseous 220Rn (t1/2 = 55.6 sec) presents a potential challenge to modeling expected increases in total radioactivity resulting from radioactive ingrowth processes. In contrast, because the half-life of 220Rn is so short, migration beyond the immediate vicinity of nuclear formation is likely minimal and disequilibrium is not expected. Thus, in this decay series, the modeled total 228Ra-supported radioactivity concentration in produced fluids has the potential to increase to a maximum within 5 years of extraction from the shale formation, followed by a decrease determined by the half-life of 228Ra (t1/2 = 5.75 years) (Figure 4A,B). This suggests that inclusion of the ingrowth and decay of 228Ra decay products (particularly 228Th) is important for development of appropriate liquid waste management.

Figure 4 - A) Line graphs of activities (y-axes) for Ra228, associated alpha, and total activity according to time (x-axes) 15 days after extraction. B) Line graphs of activities (y-axes) for Ra228, associated alpha, and total activity according to time (x-axes) 70 years after extraction.  C) Line graphs of activities (y-axes) for Ra226, Ra228, associated alpha, and total activity according to time (x-axes) 70 years after extraction.  D) Line graphs of activities (y-axes) for Ra226, associated alpha, and total activity according to time (x-axes) 15 days after extraction.  E) Line graphs of activities (y-axes) for Ra226, associated alpha, and total activity according to time (x-axes) 70 years after extraction.  F) Line graphs of activities (y-axes) for Ra226, alpha, and total activity according to time (x-axes) 5000 years after extraction.Figure 4 – Theoretical Bateman model of Ra decay product ingrowth and decay (system closed to release of gaseous radon) (A) 15 days after extraction for 228Ra (green dots), associated alpha (red dashes), and total activity (blue); (B) 70 years after extraction for 228Ra (green dots), associated alpha (red dashes), and total activity (blue); (C) 70 years after extraction for 226Ra (purple), 228Ra (green dots), associated alpha (red dashes), and total activity (blue); (D) 15 days after extraction for 226Ra (purple), associated alpha (red dashes), and total activity (blue); (E) 70 years after extraction for 226Ra (purple), associated alpha (red dashes), and total activity (blue); and (F) 5,000 years after extraction for 226Ra (purple), associated alpha (red dashes), and total activity (blue).

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238U series partitioning. Owing to the geologic history and reducing (anoxic) conditions at depth in the Marcellus Shale formation, parent and supporting radionuclide 238U (which, unlike 232Th, can be redox active under natural conditions) is likely to be contained in the crystal lattice of minerals or adsorbed to solid phase structures in a reduced highly insoluble (+4) oxidation state (Swanson 1961) (Figures 1 and 3). Thus, geochemical conditions favor adsorption of 238U and decay-product actinides (234Th, 234Pa, and 234U) to interstitial surfaces of surrounding minerals (Figures 1 and 3) (Melson et al. 2012), and these radionuclides are likely fixed at depth. In support of these assertions, we observed exceedingly low concentrations of U and Th radionuclides in unfiltered produced fluids from Marcellus Shale (Tables 1 and 2; see also Supplemental Material, “Uranium absent”). Analysis of alpha spectra further revealed an apparent enrichment of 234U (relative to 238U) in produced fluids, which can likely be explained by alpha-recoil processes (Figure 2E,F) (Fleischer 1980; Osmond et al. 1983). Further investigations of partitioning among relevant phases (filtered/ultrafiltered aqueous, particulate, and solid) will provide more detailed understanding of the speciation of actinides in unconventional drilling liquid wastes.

In contrast to low solubility of 238U-series actinides in produced fluids, 238U decay product radionuclide 226Ra (t1/2 = 1,600 years) is highly soluble in such fluids. Thus, 226Ra becomes enriched in the aqueous phase at depth relative to supporting actinides, with which 226Ra has likely been in secular equilibrium (steady state) for many millions of years (Gonneea et al. 2008). Decay product radionuclides of 226Ra are concerning because of the long half-life of 226Ra, which ensures natural production (via radioactive ingrowth) of decay products for thousands of years (Figure 4C–F). Although 226Ra is highly soluble in produced fluids, our observations suggest that 226Ra decay product radionuclides (Figures 1 and 3) are relatively insoluble under these conditions and are retained at depth by interactions with mineral phases in the interstitial environment. Although this geochemical behavior results in a very low concentration of 226Ra decay products as fluids emerge from depth, the Bateman radioactivity ingrowth equations predict that (in systems closed to the release of gaseous 222Rn) the total 226Ra-supported radioactivity concentration in produced fluids can increase by a factor > 5 (alpha-particle emissions by a factor of approximately 4) over a period of 15 days following extraction of produced fluids (Figure 4D). Importantly, radioactive ingrowth will continue for decades as longer-lived isotopes (210Pb, t1/2 = 22 years; 210Po, t1/2 = 138 days) approach radioactive equilibrium with 226Ra (at a rate related to their own half-lives; Figure 4E). As an example, we compared the Bateman equation–based radioactivity ingrowth model to the observed radioactivity concentration of alpha-emitting radionuclide 210Po in sequential analyses of unfiltered, acidified produced fluids from Marcellus Shale that were stored in a hermetically sealed container for several months. The observed increase in radioactivity concentrations of 210Po in this sample followed the predicted ingrowth under the conditions described (Figure 2A). Ingrowth of long-lived radioactive 210Pb and 210Po is important to overall risk assessments in this context because these radionuclides are potentially bioavailable and may accumulate in higher organisms (Bacon et al. 1988; Cherrier et al. 1995; Fisher et al. 1983; Heyraud and Cherry 1983). Thus, the use of 226Ra alone to predict total radioactivity concentration in liquid drilling wastes can underestimate the increase in levels that will occur over time and neglects the potential for the bioaccumulation of alpha- and beta-emitting decay product radionuclides in bacteria, plants, and higher organisms.

Similar to the decay product scenario of Th-series Ra isotope 228Ra, establishing radioactive equilibrium of decay product radionuclides with parent 226Ra is potentially confounded by the presence of a gaseous isotope (i.e., 222Rn, t1/2 = 3.82 days) in the decay series. Further, in this case the half-life of 222Rn is sufficiently long to potentially promote migration and separation (disequilibrium) from parent 226Ra in systems that are open to the atmosphere (e.g., containment ponds; Figure 3). In these cases, the modeled concentration of 226Ra decay products will need to include an assessment of 222Rn emanation and decay to accurately portray the total concentration in liquid drilling wastes and the impact of increased 222Rn and decay products to surroundings.

Conclusion

Previous reports that described the radioactivity concentration in flowback, produced fluids, and other materials associated with unconventional drilling and hydraulic fracturing focused on one element—Ra. Our projections suggest that in systems closed to the release of gaseous Rn, estimates based solely on 226Ra/228Ra will underestimate the total activity present by a factor > 5 within 15 days following extraction as Ra decay product radionuclides ingrow. The level of radioactivity (in a closed 226Ra decay product system) will continue to increase and reach a maximum approximately 100 years after extraction (Figure 4F). At this time, when the long-lived 210Pb and its decay products have reached equilibrium with 226Ra, the total radioactivity will have increased by a factor > 8. Although this projection assumes that losses of Rn and other geochemically derived disequilibria are negligible, the physical process of ingrowth begins again at any time of Ra separation (e.g., sulfate treatment at wastewater treatment plants), and the total activity unavoidably increases as decay product radionuclides ingrow. Thus, long-lived, environmentally persistent Ra decay products (228Th, 210Pb, 210Po) should be considered carefully as government regulators and waste handlers assess the potential for radioactive contamination and exposures.

NORM is emerging as a contaminant of concern in hydraulic fracturing/unconventional drilling wastes, yet the extent of the hazard is currently unknown. Sound waste management strategies for both solid and liquid hydraulic fracturing and unconventional drilling waste should take into account the dynamic nature of radioactive materials. Methods designed to remove Ra from hydraulic fracturing waste may not remove Ra decay products because these elements (Ac, Th, Pb, Bi, Po isotopes) have fundamentally different physicochemical properties (Kondash et al. 2014; Zhang et al. 2014). Future studies and risk assessments should include Ra decay products in assessing the potential for environmental contamination in recreational, agricultural, and residential areas, as well as in developing a more detailed understanding of the accumulation of these radionuclides in higher organisms.


References

Bacon MP, Belastock RA, Tecotzky M, Turekian KK, Spencer DW. 1988. Lead-210 and polonium-210 in ocean water profiles of the continental shelf and slope south of New England. Cont Shelf Res 8:841–853.

Barbot E, Vidic NS, Gregory KB, Vidic RD. 2013. Spatial and temporal correlation of water quality parameters of produced waters from Devonian-age shale following hydraulic fracturing. Environ Sci Technol 47:2562–2569.

Bateman H. 1910. The solution of a system of differential equations occurring in the theory of radioactive transformations. Proc Cambridge Philos Soc 15:423–427.

Blauch ME, Myers RR, Moore TR, Lipinski BA, Houston NA. 2009. Marcellus Shale Post-Frac Flowback Waters—Where Is All the Salt Coming from and What Are the Implications? In: Proceedings from the Society of Petroleum Engineers Eastern Regional Meeting, 23–25 September 2009, Charleston, WV. SPE-125740-MS; doi:10.2118/125740-MS.

Boyer C, Clark B, Jochen V, Lewis R, Miller CK. 2011. Shale gas: a global resource. Oilfield Rev 23:28–39.

Brown VJ. 2014. Radionuclides in fracking wastewater: managing a toxic blend. Environ Health Perspect 122:A50–A55; doi: 10.1289/ehp.122-A50.

Burnett JL, Croudace IW, Warwick PE. 2012. Pre-concentration of short-lived radionuclides using manganese dioxide precipitation from surface waters. J Radioanal Nucl Chem 292:25–28.

Carter KM, Harper JA, Schmid KW, Kostelnik J. 2011. Unconventional natural gas resources in Pennsylvania: the backstory of the modern Marcellus Shale play. Environ Geosci 18:217–257.

Cherrier J, Burnett WC, LaRock PA. 1995. Uptake of polonium and sulfur by bacteria. Geomicrobiol J 13:103–115.

Choppin GR, Liljenzin JO, Rydberg J. 2002. Radiochemistry and Nuclear Chemistry. 3rd ed. Worburn, MA:Butterworth-Heinemann.

Clark CE, Veil JA. 2009. Produced Water Volumes and Management Practices in the United States. ANL/EVS/R-09/1. Prepared by the Environmental Science Division, Argonne National Laboratory for the U.S. Department of Energy. Available: http://www.evs.anl.gov/publications/doc/​ANL_EVS__R09_produced_water_volume_repor​t_2437.pdf [accessed 17 February 2015].

Collé R, Laureano-Perez L, Outola I. 2007. A note on the half-life of 209Po. Appl Radiat Isot 65:728–730.

Cueto-Felgueroso L, Juanes R. 2013. Forecasting long-term gas production from shale. Proc Natl Acad Sci USA 110:19660–19661.

Currie LA. 1968. Limits for qualitative detection and quantitative determination. Application to radiochemistry. Anal Chem 40:586–593.

Eichrom Technologies LLC. 2009. Analytical Procedures: Lead-210 and Polonium-210 in Water. Available: http://www.eichrom.com/docs/methods/pdf/​otw01-20_pb-po-water.pdf [accessed 16 June 2015].

Finkel ML. 2011. The rush to drill for natural gas: a public health cautionary tale. Am J Public Health 101:784–785.

Fisher NS, Burns KA, Cherry R, Heyraud M. 1983. Accumulation and cellular distribution of 241Am, 210Po, and 210Pb in two marine algae. Mar Ecol Prog Ser 11:233–237.

Fleischer RL. 1980. Isotopic disequilibrium of uranium: alpha-recoil damage and preferential solution effects. Science 207:979–981.

Goldstein BD, Kriesky J, Pavliakova B. 2012. Missing from the table: role of the environmental public health community in governmental advisory commissions related to Marcellus Shale drilling. Environ Health Perspect 120:483–486; doi: 10.1289/ehp.1104594.

Gonneea ME, Morris PJ, Dulaiova H, Charette MA. 2008. New perspectives on radium behavior within a subterranean estuary. Mar Chem 109:250–267.

Gregory KB, Vidic RD, Dzombak DA. 2011. Water management challenges associated with the production of shale gas by hydraulic fracturing. Elements 7:181–186.

Haluszczak LO, Rose AW, Kump LR. 2013. Geochemical evaluation of flowback brine from Marcellus gas wells in Pennsylvania, USA. Appl Geochem 28:55–61.

Hammond DE, Zukin JG, Ku TL. 1988. The kinetics of radioisotope exchange between brine and rock in a geothermal system. J Geophys Res Solid Earth 93:13175–13186.

Harada K, Burnett WC, LaRock PA, Cowart JB. 1989. Polonium in Florida groundwater and its possible relationship to the sulfur cycle and bacteria. Geochim Cosmochim Acta 53:143–150.

Heyraud M, Cherry RD. 1983. Correlation of 210Po and 210Pb enrichments in the sea-surface microlayer with neuston biomass. Cont Shelf Res 1:283–293.

Horwitz EP, Chiarizia R, Dietz ML, Diamond H, Nelson DM. 1993. Separation and preconcentration of actinides from acidic media by extraction chromatography. Anal Chim Acta 281:361–372.

Howarth RW, Ingraffea A, Engelder T. 2011. Natural gas: should fracking stop? Nature 477:271–275.

Hunt S. 2014. Ohio EPA, Health Officials Dismiss Radioactive Threat from Fracking. The Columbus Dispatch (Columbus, OH) January 27. Available: http://www.dispatch.com/content/stories/​local/2014/01/27/radioactive-threat.html [accessed 2 June 2015].

Inn KGW, Hall E, Woodward JT, Stewart B, Pöllänen R, Selvig L, et al. 2008. Use of thin collodion films to prevent recoil-ion contamination of alpha-spectrometry detectors. J Radioanal Nucl Chem 276(2):385–390.

Kargbo DM, Wilhelm RG, Campbell DJ. 2010. Natural gas plays in the Marcellus Shale: challenges and potential opportunities. Environ Sci Technol 44:5679–5684.

Kerr RA. 2010. Energy. Natural gas from shale bursts onto the scene. Science 328:1624–1626.

Knight AW, Eitrheim ES, Nelson AW, Nelson S, Schultz MK. 2014. A simple-rapid method to separate uranium, thorium, and protactinium for U-series age-dating of materials. J Environ Radioact 134:66–74.

Kondash AJ, Warner NR, Lahav O, Vengosh A. 2014. Radium and barium removal through blending hydraulic fracturing fluids with acid mine drainage. Environ Sci Technol 48:1334–1342.

Libes S. 1992. An Introduction to Marine Biogeochemistry. 1st ed. New York:John Wiley and Sons.

Lutz BD, Lewis AN, Doyle MW. 2013. Generation, transport, and disposal of wastewater associated with Marcellus Shale gas development. Water Resour Res 49:647–656.

Manickam E, Sdraulig S, O’Brien R. 2010. An improved and rapid radiochemical method for the determination of polonium-210 in urine. Aust J Chem 63:38–46.

Melson NH, Haliena BP, Kaplan DI, Barnett MO. 2012. Adsorption of tetravalent thorium by geomedia. Radiochim Acta 100:827–832.

Moore WS. 1976. Sampling 228Ra in the deep ocean. Deep Sea Res Oceanogr Abstr 23:647–651.

Nelson AW, May D, Knight AW, Eitrheim ES, Mehrhoff M, Shannon R, et al. 2014. Matrix complications in the determination of radium levels in hydraulic fracturing flowback water from Marcellus Shale. Environ Sci Technol Lett 1:204–208.

NNDC (National Nuclear Data Center). 2013. NuDat 2 Database. Available: http://www.nndc.bnl.gov/nudat2/ [accessed 17 February 2015].

Nour S, El-Sharkawy A, Burnett WC, Horwitz EP. 2004. Radium-228 determination of natural waters via concentration on manganese dioxide and separation using Diphonix ion exchange resin. Appl Radiat Isot 61:1173–1178.

Osborn SG, McIntosh JC. 2010. Chemical and isotopic tracers of the contribution of microbial gas in Devonian organic-rich shales and reservoir sandstones, northern Appalachian Basin. Appl Geochem 25:456–471.

Osmond JK, Cowart JB, Ivanovich M. 1983. Uranium isotopic disequilibrium in ground water as an indicator of anomalies. Int J Appl Radiat Isot 34:283–308.

Rowan EL, Engle MA, Kirby CS, Kraemer TF. 2011. Radium Content of Oil- and Gas-Field Produced Waters in the Northern Appalachian Basin (USA): Summary and Discussion of Data. Scientific Investigations Report 2011–5135. Available: http://pubs.usgs.gov/sir/2011/5135/pdf/s​ir2011-5135.pdf [accessed 17 February 2015].

Schmidt CW. 2011. Blind rush? Shale gas boom proceeds amid human health questions. Environ Health Perspect 119:A348–A353; doi: 10.1289/ehp.119-a348.

Swanson VE. 1961. Geology and Geochemistry of Uranium in Marine Black Shales: A Review. Available: http://pubs.usgs.gov/pp/0356c/report.pdf [accessed 8 June 2014].

Thompson H. 2012. Fracking boom spurs environmental audit. Nature 485:556–557.

U.S. Energy Information Administration. 2014. Annual Energy Outlook 2014 Early Release. Available: http://www.eia.gov/forecasts/aeo/er/pdf/​0383er%282014%29.pdf [accessed 8 June 2014].

Vengosh A, Jackson RB, Warner N, Darrah TH, Kondash A. 2014. A critical review of the risks to water resources from unconventional shale gas development and hydraulic fracturing in the United States. Environ Sci Technol 48(15):8334–8348; doi: 10.1021/es405118y.

Vidic RD, Brantley SL, Vandenbossche JM, Yoxtheimer D, Abad JD. 2013. Impact of shale gas development on regional water quality. Science 340:1235009; doi: 10.1126/science.1235009.

Warner NR, Christie CA, Jackson RB, Vengosh A. 2013. Impacts of shale gas wastewater disposal on water quality in western Pennsylvania. Environ Sci Technol 47:11849–11857.

Yang H, Flower RJ, Thompson JR. 2013. Shale-gas plans threaten China’s water resources. Science 340:1288; doi: 10.1126/science.340.6138.1288-a.

Zhang T, Gregory K, Hammack RW, Vidic RD. 2014. Co-precipitation of radium with barium and strontium sulfate and its impact on the fate of radium during treatment of produced water from unconventional gas extraction. Environ Sci Technol 48:4596–4603.


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