Characterization of Naturally Occurring Radioactive Material (NORM) Generated from the Lower Cretaceous Carbonate Formations in the Arabian Peninsula and Gulf
Authors:
Francesco Arneodo, Marco Balata, Mohamed Lotfi Benabderrahmane, Gianmarco Bruno, Adriano Di Giovanni, Osama Fawwaz, Matthias Laubenstein, Laura Manenti, Stefano Nisi, Dipl.-Ing. Dr.mont. Rüdiger B. Richter, MSRP
For most of the petroleum reservoirs in the world, the impact of the mother nuclides such as uranium-238 on the deposition of radioactive materials a.k.a. NORM from the formation and particularly as mineral scales adherent to tubulars and other equipment is considered insignificant. Uranium is regarded as insoluble in the reservoir formation and the prevailing understanding is that dissolved radium is not generated necessarily by U and Th in solution. Consequently, “uranium scale”, as a technical term, seems to be non-existent in the oil and gas industry. However, gamma spectroscopy and chemical analysis of NORM scale samples of carbonate origin, performed in the course of this research, has proven that they actually can contain uranium. A fundamental relationship between uranium and vanadium in scales is presumed. The highest specific activity of 238U in scale analyzed with gamma spectroscopy was at 11.4 [Bq/g] and supplementary chemical analysis has shown concentrations of up to 740 ppm total uranium and up to 260 ppm vanadium.
Notes
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1 Introduction
Naturally Occurring Radioactive Material (NORM), as a characteristic oil and gas waste, is usually generated in the stage of production, but occasionally also during drilling of exploration wells. The presence of NORM in the oil and gas industry has been reported earlier by various authors [1‐5]. The source of NORM are radionuclides and particularly their water-soluble radiochemical compounds which exist naturally in the geological formation of the hydrocarbon reservoir. The primary radioisotopes of concern are of the uranium-radium decay series (238U), the thorium (232Th) decay series and potassium (40K) which occur freely in the earth’s crust [6, 7]. Not frequently reflected for the evaluation of NORM is the actinium (235U) decay series [8]. Radioisotopes would naturally be in secular equilibrium if remaining undisturbed for a long enough timeline, but owing to the possible migration of some radionuclides into a mineral matrix and getting deposited at different locations, these radionuclides may become “unsupported”, and hence have an activity different from their parents in the decay chain [9]. The concentrations of uranium and thorium in the earth’s crust is 4.2 and 12.5 ppm, respectively [10]. Both won’t appear, as per the prevailing opinion, in significant quantities in NORM samples, because they are commonly considered relatively stable, which means that they mainly occur in form of water-insoluble minerals [11].
Water-soluble compounds of naturally occurring radionuclides, particularly radium compounds, throughout their passage via naturally radioactive geological stratigraphic horizons such as bedrock and shale will leach into the formation water [12]. This is particularly the case in the Middle East, where carbonates and sandstone prevail. Water comes to the surface along with the pumped crude as an oil/produced water mixture, where the dissolved mineral salts precipitate and form less soluble minerals in scales but also in sedimentation areas as sludge [13], as shown in Fig. 1.
Fig. 1
Typical pathways of NORM accumulation in the oil and gas industry (modified from [14])
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The main types of NORM from the oil and gas industry as shown in Fig. 1 are, therefore:
Mineral scales, deposits and thin films (radon progeny) accumulate in plant equipment and particularly adherent to tubular (drill pipes, casings and tubulars); and
Petroleum hydrocarbon (PHC)-sludge and scrapings from cleaning and pigging activities, which contain radioactive mineral solids.
1.1 Mineral Scale
Scale appears as a mineral layer accumulated inside pipes, separators, filters, pumps, wellheads (aka. Christmas trees) and other equipment, as a result of precipitating newly formed (formerly soluble) radionuclide compounds in the produced water. Precipitation is mainly due to changes in pressure and temperature [7], but mechanical impacts also play a role and the amount of the precipitate depends on the physical and chemical properties of the produced water (brine) [15] such as salinity, or pH level [16]. The highest concentrations of NORM are typically found in scale deposits that form under certain physical and chemical conditions when dissolved radionuclide compounds co-precipitate together with barite and celestite (BaSO4 and SrSO4, respectively) and/or aragonite (CaCO3). These sulfates and carbonate, after generation from the minerals dissolved in the brine/produced water, form insoluble scales but also deposits of high density (often confused with mineral hardness), on the inside of tubulars and production or exploration equipment. Just like calcium, strontium and barium, radium also belongs to the alkaline earth metals (2nd group of the PSE) and hence radium has geochemical affinities to similar elements. It co-precipitates with them forming radium sulfate (RaSO4) and particularly mixed sulfates within the Ra–Ba, Ra–Sr and the Ra–Ba–Sr system. These sulfate scales commonly do not contain uranium. However, under alkaline conditions radium carbonate (RaCO3) in particular, but also radium silicate (RaSiO3) may be generated [17‐19]. Under these correspondingly alkaline conditions the formation of “uranium scale” occurs as shown as a result of this research.
1.2 NORM Sludge
Sludge is an oily residue that accumulates at the bottom of storage tanks and other production equipment, particularly in separators. Sludge is made of deposits from heavy hydrocarbons, tight emulsions, produced formation sand and small quantities of corrosion and flaking debris that settle out of suspension in some field equipment [13]. Sludge from pipeline pigging is also addressed as scrapings. NORM in sludge accumulates when radium co-precipitates with silicates and carbonates [9, 20, 21]. The specific activity of radium-226 in sludge can reach values of up to 3500 Bq/g [22].
1.3 Lead Films
Films, as shown in Fig. 1, are very thin layers that contain mostly the daughter nuclides of radon (222Rn; t1/2 = 3.8 days) such as bismuth (214Bi; t1/2 = 19.9 min), lead (210Pb; t1/2 = 22.2 years) and polonium (210Po; t1/2 = 138.4 days). Highly variable ranges of specific activities were measured for scales and can be as high as 15,000 Bq/g for 226Ra [22]. 210Pb and 210Po are also found in films inside gas pipes, gas/oil separators, liquid natural gas storage tanks, in sludge accumulating in tank bottoms, dehydration vessels, and in waste pits in addition to crude oil pipeline scrapings [11].
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1.4 Black Dust
Black dust (black powder), as a corrosion product of pipe material together with possibly adhered lead films in gas transmission pipelines, commonly contains 210Pb but also mercury, which is associated to thiols (mercaptans) in the gas reservoir or condensate. These waste types are not subject of this paper which focusses in particular on mineral scales from oil production and exploration.
1.5 Hazards of NORM
Radioactive wastes associated with the exploration and production of oil and gas are considered carcinogenic, mutagenic and teratogenic; they are harmful to humans, animals and the environment [23]. These NORM wastes shall be managed in such a way that they do not affect human health and the environment. More recent technical options for treatment, removal and decontamination of NORM- and TENORM-contaminated equipment and debris were published earlier [17, 24‐26]. TENORM, as a technical term, describes in particular technologically enhanced NORM, which is rather generated in specific downstream operations such as ethylene cracking etc. than in offshore operations.
1.6 Objective of this Paper
The objective of this paper is the characterization of NORM scales from carbonate-rich limestone dominated geological formations which consequently will have a different radiochemical and chemical composition, in particular, the formation of ‘uranium scale’, in contrast to NORM scales generated from other facies, as mentioned above.
2 Theory
2.1 Existence and Origin of Soluble Uranyl Minerals in Carbonate Formation Rocks
The Lower Cretaceous Formations in the Arabian Peninsula and Gulf appear to a high extent to be of carbonate origin [27‐30]. From the relevant literature concerning the appearance of NORM-scales, it corresponds to the general view, that usually only the daughter nuclides of the uranium (238U), thorium (232Th) and the actinium (235U) decay series are present. Owing to the low solubility of uranium compounds in water such as tri-uranium octoxide (U3O8) in the formation concerned [7, 31] and the current understanding, that dissolved radium is not generated by U and Th in solution [32]. Consequently, the characterization as “radium-rich scale”, a.k.a. “radium scale” [6, 33] is widely used, whilst the term ‘uranium scale’ seems to be fundamentally unknown in the oil and gas industry.
Uranium in its compounds usually exists in valences of +2, +3, +4, +5, and +6. In aqueous solution, only ions having a valence of +4 and +6, exist. The redox behaviour of uranium allows to transfer tetravalent into hexavalent uranium, simply by oxidation in an aqueous solution:
U6+ is the most stable species of uranium and exists predominantly as uranyl cation (UO2)2+, whilst in sodic alkaline carbonate enriched solutions, U6+ is available as uranyl tricarbonate complex [UO2 (CO3) 3]4− (Fig. 2).
Fig. 2
Pourbaix-diagrams of uranium in water (left) and in a carbonate environment (right) [34]
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The most plausible reason for the migration of commonly stable uranium oxides into the environment and the generation of uranium-bearing NORM scales is the formation of uranyl carbonate and hydroxide minerals and their ability to be more water-soluble as mixed complex ions such as (UO2)2CO3(OH)3− [35, 36].
In particular, the presence of the carbonate ion CO32− has considerably high impact on the solubility of uranium owing to the formation of uranyl carbonate complexes such as uranium dicarbonate UO2(CO3)22− and uranium tricarbonate UO2(CO3)34−. Whilst the solubility product of Rutherfordine (UO2)CO3 with Ksp = 10−16.4 (mol/l)3 is still very low (almost water insoluble), the solubility product of uranium dicarbonate UO2(CO3)22− with Ksp = 10+20.4 (mol/l)3 and for uranium tricarbonate UO2(CO3)22− with Ksp = 10+24.2 (mol/l)3 demonstrates excellent solubility in water [37].
Limestone, dolomites and other sedimentary carbonate rocks have been considered earlier as non-uraniferous [37]. However, carbonate-cemented calcretized sediments host large surficial uranium deposits [37‐40], where in particular the formation of ‘uranovanadates’ is considered a major criterion for the genesis of such deposits [41, 42]. Relevant members of the carnotite group and other double salts of the uranyl cation are listed in Table 1.
TABLE 1
Uranovanadate minerals of the carnotite group and related species [43‐45]
Mineral Name
Mineralogical Formula (IMA)
Crystal System
Carnotite
K2(UO2)2(VO4)2 · 2–3H2O
Monoclinic
Strelkinite
Na2(UO2)2(VO4)2 · 6H2O
Orthorhombic
Tyuyamunite
Ca(UO2)2(VO4)2 · 5–8H2O
Orthorhombic
Metatyuyamunite
Ca(UO2)2(VO4)2 · 3–5H2O
Orthorhombic
Vanuralite
Al(UO2)2(V2O8)(OH) · 11H2O
Monoclinic
Metavanuralite
Al(UO2)2(VO4)2(OH) · 8H2O
Triclinic
Margaritasite
(Cs,K,H3O)2(UO2)2(VO4)2 · H2O
Monoclinic
Sengierite
Cu2(UO2)2(VO4)2(OH) 2 · 6H2O
Monoclinic
Vanuranylite
(H3O)2(UO2)2(VO4)2 · 4H2O
Monoclinic
Curienite
Pb(UO2)2(VO4)2 · 5H2O
Orthorhombic
Francevillite
(Ba,Pb)(UO2)2(VO4)2 · 5H2O
Orthorhombic
Fritzscheite
Mn(UO2)2(PO4,VO4)2 · 10H2O
Tetragonal
More recent articles concerning the appearance of uranyl vanadates in carbonates and calcretes, particularly in countries of the Middle East, were published for a study area in Central Jordan by Koury et al. [46]. Pracejus and his co-workers [47] also published a paper concerning tertiary limestone and calcretes in Southern Oman. Consequently, secondary formed uranovanadate minerals may act as a source of soluble uranium in formation water, particularly in a carbonate environment. The solubility of carnotite in carbonated water is about three orders higher than in pure water [48]. Also, the existence of uranyl selenites may play a role in the generation of uranium scales. Although their crystal structures (mineralogical habit) has only recently been discovered [49] and being rather unknown in nature, uranyl selenates have high solubility in aqueous solutions and Se6+ is easily reduced to Se4+ under common natural conditions [50, 51].
2.2 Description of the Study Area and Origin of the NORM Samples
The Upper Jurassic Carbonate Formations (Arab A, B, C and the Upper Arab D) and the Middle Jurassic Araej Formation host the rich oil reservoirs in the Kingdom of Saudi Arabia, the United Arab Emirates (particularly Western Abu Dhabi), the State of Qatar and the Kingdom of Bahrain. Limestone, dolomite and anhydrite are the three major rock types of the Arab Formations [27]. The reservoir conditions in the Araej Formation are dominated by limestone facies [28]. These elder formations are overlaid offshore Central Abu Dhabi by the Lower Cretaceous Kharaib Formation including the Thamama Group. Particularly Zone 4 of the latter is the most important producer for the giant Upper Zakum oil field. The Thamama Group consists of three discrete porous chalky limestone units, which are each underlain by dense argillaceous limestone [29, 30]. The NORM samples which are subject of this study are entirely assigned to these ‘Lower Cretaceous Formations’.
3 Experimental and Interpretation of Analysis Results
3.1 Gamma-ray Spectroscopy
Gamma-ray spectroscopy (gamma spectroscopy) is a key technology for the quantitative study and analysis of the energy spectra of gamma-ray emitters. The measuring arrangement typically consists of a scintillator that emits a pulse of light when interacting with a gamma-ray, a photomultiplier that converts and amplifies the light pulse into a current pulse, and the subsequent amplifiers and counters. In the course of the present research a NaI(Tl) scintillation radiation detector, using a single crystal of thallium doped sodium iodide, and a high purity germanium (HPGe) detector were applied.
3.1.1 Gamma Spectroscopy Applying a NaI(Tl) Scintillation Radiation Detector
26 scale samples were measured, as collected from the field (slowly dried at ambient temperature), without any further treatment. An ORTEC, 3 × 3 inch—905 Series NaI(Tl) scintillation radiation detector, coupled to a digiBASE 14-Pin PMT Base, with Integrated Bias Supply, Preamplifier, and MCA with Digital Signal Processing, was used. Sampling was automated for 12 h acquisition time using the ‘MAESTRO Multichannel Analyzer Emulation’. The analysis was carried out using the ORIGIN® 2018 graphing and analysis software.
The absolute efficiency of the detector was calculated based on the activity of 40K, using a potassium chloride sample [52], and found to be 5.024 ± 0.014% at 1460.82 keV. The efficiency curve for the NaI(Tl) detector was produced using GEANT4 simulation [53] and then normalized to match the measured value for 40K.
The detector was calibrated by using a low activity sample, prepared in the lab using “Gas Light Lamp Mantle” containing thorium (232Th), mixed with organic brown sugar, which was also used for recording the background radiation. It also showed a quite similar geometry to that of the NORM samples. The detector’s resolution at 609 keV was 7.90 ± 0.05%. The radionuclides studied in this work were 226Ra (1600 y), 214Pb (26.8 min), 214Bi (19.9 min), 234Th (24.1 days) and 235U (7.038 × 108 y). The spectra produced by the NaI detector indicated no evidence of 228Th or 40K activity beyond the critical limit.
From 26 samples analyzed, 9 samples had no detectable activity, and hence the activity of any possibly present radioisotope was below detection limits. Ten samples contained 226Ra and its progeny, and seven of the samples contained 235U and 238U but not 226Ra, 228Ra or 232Th and their progenies.
Survey of 226-Radium and Its Progeny
For this survey, only 226Ra and its progeny were examined, using the NaI(Tl) detector. The lines of 226Ra at 186.211 keV (3.64%), 214Pb at 351.9321 keV (35.6%) and 214Bi at 609.32 keV (45.49%) were analyzed for specific activity measurement. For closed isotopic systems, the secular equilibrium between the parent-daughter radionuclide can be attained after a period equivalent to approx. 6 times 10 half-lives of the daughter nuclide, where no parent decay occurs [54] (~20 h in the case of 214Bi). Comparable activities were noted for 214Bi and 214Pb for the higher activity samples (5 to 10 times higher). These samples had no measurable activity for the 228Ra progeny (daughters of 232Th) and 40K. Uncertainties, also shown in Table 2 (and later on, Table 3), are obtained by combining components from peak fitting and the sample’s mass measurement.
TABLE 2
Specific activity of 226Radium, 214Lead and 214Bismuth
Sr. No
Sample Name
226Ra
[Bq/g]
214Pb
[Bq/g]
214Bi
[Bq/g]
1
SCALE-A-67
23.5 ± 0.3
14.1 ± 0.3
10.4 ± 0.4
2
SCALE-A-68
8.4 ± 0.2
5.1 ± 0.1
2.9 ± 0.1
3
SCALE-A-73
2.9 ± 0.1
2.04 ± 0.02
1.42 ± 0.03
4
SCALE-A-75
1.5 ± 0.2
0.66 ± 0.02
0.49 ± 0.03
5
SCALE-B-42
50 ± 1
39 ± 2
35 ± 2
6
SCALE-B-44
145 ± 4
110 ± 3
105 ± 3
7
SCALE-B-48
53 ± 2
42 ± 1
39 ± 1
8
SCALE-B-61
51 ± 2
36 ± 1
39 ± 1
9
SCALE-B-63
33 ± 1
25 ± 1
24 ± 1
10
SCALE-B-64
36 ± 1
33 ± 1
32 ± 1
TABLE 3
Specific activity of 235Uranium and 234Thorium
Sr. No
Sample Name
235U
[Bq/g]
234Th
[Bq/g]
1
SCALE-A-69
0.25 ± 0.02
5.2 ± 0.2
2
SCALE-A-70
0.46 ± 0.04
9.5 ± 0.5
3
SCALE-A-72
0.36 ± 0.04
6.2 ± 0.4
4
SCALE-A-80
0.26 ± 0.02
4.4 ± 0.2
5
SCALE-A-82
0.35 ± 0.07
9 ± 2
6
SCALE-B-34
0.41 ± 0.04
11.5 ± 0.4
7
SCALE-B-35
0.36 ± 0.01
8.6 ± 0.4
Previous work studying the equilibrium in NORM samples has shown that 226Ra activity was almost always inferred from 214Pb and 214Bi [55, 56]. Consequently, a possible interpretation for the higher values obtained could be the interference from 235U line at 185.715 keV (57%). (Table 2).
In Fig. 3 the 226Ra spectrum is shown with the three lines used for activity calculation, using the example of sample SCALE-B-42.
Fig. 3
226Ra spectrum showing the three lines used for activity calculation
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Survey of 235/238-Uranium and Its Progeny
No significant activity is present for 226Ra or 232Th and their progenies in these samples. The evaluation of the 238U activity has been done using its daughter 234Th (24.10 d), a peak that is a combination of the lines 92.38 and 92.80 keV with intensities 2.13 and 2.1%, respectively. It was not possible to use the 1001.03 keV line from 234mPa which is highly favoured for uranium measurement [57] due to detector resolution and its low intensity (0.842%). 235U activity was evaluated using the line at 185.715 keV (57%). Such a spectrum is usually obtained in water treatment/purification facilities. A similar spectrum was reported for IONEX resin, a material used in filters which is ‘highly selective for uranium’ ([58]; Table 3).
In Fig. 4 the 238/235U spectrum is shown with the two lines used for activity calculation, using the example of sample SCALE-B-34.
Fig. 4
238/235U spectrum showing the two lines used for activity calculation of sample SCALE-B-34
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3.1.2 Gamma Spectroscopy Applying a High Purity Germanium (HPGe) Radiation Detector
Owing to the limited energy resolution of NaI(Tl) detectors, the analysis can be quite difficult and hampered by the natural limitations of the process, especially for multiplet structures where multiple gamma lines sometimes interfere with X‑rays in certain peaks. Three of the already measured (with the NaI(Tl) detector) scale samples (A-67, A‑68 and A‑72) were re-measured at the ‘Laboratori Nazionali del Gran Sasso (LNGS)’, using HPGe (high purity germanium) GeDSG detector for an acquisition time of more than 24 h (Tables 4 and 5).
TABLE 4
HPGe activity results of 235Uranium and 234Thorium; NaI(Tl) results are in bold for comparison
234Th
[Bq/g]
234Th
[Bq/g]
234mPa
[Bq/g]
234U
[Bq/g]
235U
[Bq/g]
235U
[Bq/g]
SCALE-A-72
8.9 ± 0.7
6.2±0.4
8.2 ± 0.6
8.6 ± 0.9
0.42 ± 0.03
0.36±0.04
228Th (daughter of 232Th) activity was 0.8 ± 0.4 Bq/kg, and 40K was less than 4.9 Bq/kg
TABLE 5
HPGe activity results of scale samples A‑67 and A‑68; NaI(Tl) results are in bold for comparison
SCALE-A-67
SCALE-A-68
226Ra [Bq/g]
14.9 ± 0.6
3.95 ± 0.16
226Ra [Bq/g]
23.5±0.3
8.4±0.2
214Pb [Bq/g]
14.1±0.3
5.1±0.1
214Bi [Bq/g]
10.4±0.4
2.9±0.1
234Th [Bq/g]
7.28 ± 0.39
5.35 ± 0.29
234mPa [Bq/g]
7.6 ± 0.8
5.2 ± 0.5
235U [Bq/g]
0.34 ± 0.03
0.24 ± 0.18
210Pb [Bq/g]
1.83 ± 0.14
<12
228Ra [Bq/g]
0.026 ± 0.009
0.011 ± 0.004
40K [Bq/g]
<0.057
<0.025
226Ra was inferred from 214Pb & 214Bi, and 228Ra from 228Ac
The activity measured with the NaI (Tl) detector was close to the results of the HPGe measurement and several times in agreement. Good conformity with the results of the HPGe has been shown in particular for well isolated lines, having less neighbouring interference. The more recent literature refers to examples of good agreement [58], but also to some discrepancies in other cases [59]. Fig. 5 shows the spectra of samples measured with both the NaI(Tl) and the HPGe detector.
Fig. 5
Spectra of samples measured with both the NaI(Tl) and the HPGe detector
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3.2 Chemical Analysis and Mineralogical Interpretation
In addition to a radiological examination, a chemical analysis of all relevant metals is essential for complete characterization.
3.2.1 Visual Pre-examination of Selected Scale Samples
The visual appearance of the same three samples analyzed by HPGe (A-67, A‑68 and A‑72) is shown in Fig. 6. Iron, mainly from the corrosion of steel, is the dominating metal, which is also reflected in the analysis results (Table 7). The matrix of the scale is carbonate, mainly ferrous carbonate such as antiferromagnetic siderite FeCO3. A minor fraction appears to be goethite (α-FeOOH) which was not fully migrated into the existing carbonate matrix. Radium exists mainly as radium carbonate, namely as Ra-Ba-carbonate, and to a minor extent also Ra-Ba-sulfate which is overgrown/embedded within the mentioned Iron(II)-carbonate matrix.
Fig. 6
Visual appearance of the scale samples A‑67, A‑68 and A‑72
Scale samples A‑67, A‑68 and A‑72 were also undergoing a full semiquantitative multi-element metal and metalloid analysis by ‘Inductively Coupled Plasma Mass Spectrometry (ICP MS)’ at ‘Laboratori Nazionali del Gran Sasso’ (Tables 6, 7 and 8).
TABLE 6
Summary of the samples list and dissolution procedure applied
Sample Name
Mass [mg]
Wet digestion procedure
Total Dilution Factor
SCALE-A-67
0.2745
5 ml conc. HNO3(69% w/w) + 2 ml conc. HCl (37% w/w) + 0.5 ml conc. HF (49% w/w) in ultrasonic bath for 2 days at 60 °C
5464
SCALE-A-68
0.2639
5684
SCALE-A-72
0.2781
5394
TABLE 7
Semiquantitative analysis of metals and metalloids by ICP-MS
SCALE-A-67 [ppb]
SCALE-A-68 [ppb]
SCALE-A-72 [ppb]
SCALE-A-67 [ppb]
SCALE-A-68 [ppb]
SCALE-A-72 [ppb]
Fe
2.1E + 08
2.9E + 08
3.2E + 08
Li
4.3E + 04
2.5E + 04
1.7E + 04
Sr
8.6E + 07
2.1E + 07
4.0E + 04
Sb
8.4E + 03
1.0E + 04
2.8E + 03
Ca
5.3E + 07
1.7E + 07
7.0E + 06
Ge
6.7E + 03
9.5E + 03
9.5E + 03
Ba
7.2E + 06
7.0E + 06
7.3E + 04
B
1.0E + 04
6.4E + 03
4.8E + 03
Mn
2.2E + 06
3.0E + 06
4.0E + 06
Rb
8.4E + 02
1.1E + 03
1.0E + 03
Cr
5.6E + 06
1.5E + 06
5.1E + 05
Ce
9.0E + 02
8.1E + 02
3.1E + 02
Mg
2.3E + 06
1.1E + 06
2.3E + 06
La
6.2E + 02
6.4E + 02
1.8E + 02
Zn
1.5E + 06
6.8E + 05
1.7E + 05
Eu
5.8E + 02
5.5E + 02
<21.00
Cu
5.9E + 05
5.4E + 05
7.2E + 04
Y
1.0E + 03
4.7E + 02
1.6E + 02
Al
5.7E + 05
5.3E + 05
4.1E + 05
Th
1.7E + 02
1.5E + 02
1.1E + 02
U
6.8E + 05
4.9E + 05
6.8E + 05
Gd
1.5E + 02
1.4E + 02
<68.00
Ga
3.1E + 05
3.1E + 05
5.7E + 03
Bi
2.4E + 02
1.3E + 02
9.9E + 01
Ni
2.6E + 05
3.1E + 05
1.2E + 05
Sm
1.0E + 02
1.2E + 02
<81.00
Na
6.5E + 05
2.8E + 05
3.9E + 05
Pr
9.5E + 01
1.0E + 02
3.0E + 01
K
2.7E + 05
2.3E + 05
2.4E + 05
Ag
1.6E + 02
8.5E + 01
4.3E + 01
V
2.6E + 05
2.2E + 05
2.2E + 05
Cs
2.9E + 01
5.1E + 01
8.8E + 01
Se
2.2E + 05
1.9E + 05
1.6E + 05
Ho
1.1E + 01
1.1E + 01
<10.00
Co
1.4E + 05
1.4E + 05
2.4E + 05
Er
3.9E + 01
<34.00
<32.00
As
6.9E + 04
1.0E + 05
2.1E + 04
Sc
<2000
<2000
<2000
Mo
5.6E + 04
9.5E + 04
1.8E + 04
Cd
<170.0
<180.0
4.7E + 02
Pb
5.2E + 04
7.1E + 04
1.9E + 05
Tb
1.7E + 01
<10.00
<10.00
TABLE 8
Total thorium and total uranium analyzed by ICP-MS
SCALE-A-67
SCALE-A-68
SCALE-A-72
Th [ppm]
0.19
0.13
0.12
U [ppm]
740
470
700
The concentration values refer to the solid samples the uncertainty is about 30% of the given values
With regard to the quantitative analysis, the instrument was calibrated using a certified standard solution containing 10 ppb of Li, Y, Ce, Tl. The uncertainty in this working mode (semi-quantitative analysis) is about 30% of the given concentration values. A reagent blank was also measured and its signal was subtracted from the sample signals. The results are shown in Table 7. The concentration values refer to solid dry samples.
The clearly demonstrated existence of transition metals such as copper, lead and vanadium in the analyzed scale (Table 7), allows conclusions to be drawn towards uranovanadates (see Table 1) as being a possible source. Table 9 shows estimates of the order of magnitude of relevant uranium-transition metal ratios calculated from Tables 7 and 8 and relates to the entire uranium analyzed.
TABLE 9
Uranium-transition metal ratios calculated from Tables 7 and 8
Carnotite K2(UO2)2(VO4)2 · 3H2O has a vanadium-uranium ratio of 1:4.67,
Sengierite Cu2(UO2)2(VO4)2(OH)2 · 6H2O has a copper-uranium ratio of 1:3.75,
Curienite Pb(UO2)2(VO4)2 · 5H2O has a lead-uranium ratio of 1:2.30.
An exact assignment to individual transition metals or minerals is not directly possible. However, this comparison indicates a possible trend and shows an apparently good match for sengierite, whilst carnotite seems not to be the only possible source for vanadium and the appearance of lead can be allocated to curienite, because the lead–uranium ratio of the mineral is fitting into the lead–uranium ratio of the scale samples.
3.2.3 Uranium Isotopic Ratio Measurements
To perform U isotopic measurements, the same solution had been analyzed. The instrumental mass bias was corrected by 50 ppb of natural uranium isotopic reference material (IRMM-3184). (Table 10).
TABLE 10
U Isotopic composition measured in the scale samples
234U/Tot [%]
235U/Tot [%]
238U/Tot [%]
SCALE-A-67
0.0055 ± 0.0003
0.711 ± 0.010
99.28 ± 0.02
SCALE-A-68
0.0058 ± 0.0005
0.715 ± 0.010
99.28 ± 0.03
SCALE-A-72
0.0059 ± 0.0003
0.714 ± 0.010
99.28 ± 0.02
IRMM-3184
0.0052752
0.72096
99.27376
The abundance ratio of the isotopes (235U/238U) as a natural rule is 7.257E-03 [60]. The resulting ratio for the reference material in Table 10 of 7.262E-03 demonstrates good agreement and acceptable accuracy.
4 Summary and Outlook
In the course of this study, it was proven several times by radiological and chemical analysis that uranium definitely exists in NORM-bearing mineral scales. The highest specific activity of 238U analyzed in the subject scale samples with gamma spectroscopy was 11.4 [Bq/g] and supplementary chemical analysis has shown concentrations of total uranium of up to 740 ppm, which is still far below the exploitable limit of uranium mines. However, the technical term ‘uranium scale’ is justified.
The very likely existence of uranovanadates such as carnotite K2(UO2)2(VO4)2·2–3H2O and other minerals of the carnotite group and related species as a typical appearance of calcrete hosted uranium deposits and their increased aqueous solubility in carbonate environments are considered a possible source for the generation of ‘uranium scale’ in oil production equipment from the Lower Cretaceous Carbonate Formations in the Middle East.
Based on the results of this study, scale removal from tubulars and equipment (descaling), which is a relevant issue in the oil and gas industry, is not possible with chemical solvents or acids owing to the insoluble siderite matrix of the scale. Consequently, wet-mechanic pipe cleaning technologies may be applied such as high-pressure jet cleaning either with or without supportive abrasives. Processing of NORM scale after removal from the equipment with the typical technologies known from ore processing such as milling and flotation [61] is conceivable, but currently fails due to low available quantities and economic viability as well as the lack of recycling and disposal options for the generated waste streams.
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Characterization of Naturally Occurring Radioactive Material (NORM) Generated from the Lower Cretaceous Carbonate Formations in the Arabian Peninsula and Gulf
Authors
Francesco Arneodo Marco Balata Mohamed Lotfi Benabderrahmane Gianmarco Bruno Adriano Di Giovanni Osama Fawwaz Matthias Laubenstein Laura Manenti Stefano Nisi Dipl.-Ing. Dr.mont. Rüdiger B. Richter, MSRP
