Difference between revisions of "OR/17/001 The distribution of natural radioactivity in rocks"
m (1 revision imported)
|Line 150:||Line 150:|
Most of the daughter isotopes of <sup>232</sup>Th are very short-lived but <sup>228</sup>Ra (half-life 5.75 years) can be an important component in some NORM wastes.
Most of the daughter isotopes of <sup>232</sup>Th are very short-lived but <sup>228</sup>Ra (half-life 5.75 years) can be an important component in some NORM wastes.
[[Image:OR17001fig2.jpg|thumb|center|500px| '''Figure 2''' Schematic drawing of the 232Th decay chains showing the decay path and radionuclide half-life (nuclide half-life data taken from Bourdon et al., 2003<ref name="Bourdon 2003">
[[Image:OR17001fig2.jpg|thumb|center|500px| '''Figure 2''' Schematic drawing of the 232Th decay chains showing the decay path and radionuclide half-life (nuclide half-life data taken from Bourdon et al., 2003<ref name="Bourdon 2003"></ref>).]]
Revision as of 13:42, 3 December 2019
|Tye, A M, Milodowski, A E, and Smedley, P L. 2017. Distribution of natural radioactivity in the environment. British Geological Survey Internal Report, OR/17/001.|
The principal naturally-occurring radioactive elements that contribute the majority of the background radioactivity in rocks are uranium (U), thorium (Th) and potassium (K).
Uranium and its daughter radionuclides
Uranium has three natural isotopes: 238U, 235U and 234U (Wedepohl, 1978a). All three isotopes are radioactive, and 238U and 235U are the progenitor parent isotopes for two separate decay series, which ultimately lead to the formation of the lead daughter isotopes 206Pb and 207Pb, respectively (Figure 1). 238U is the most abundant isotope, and the 238U/235U ratio today is 137.5 ± 0.5 (Wedepohl, 1978a). This ratio has increased over time due to faster radioactive decay of 235U (half-life; 7.04 x 108 years) relative to 238U (half-life 4.47 x 109 years). 234U, which is produced by the decay of 238U and has a relatively short half-life (2.45 x 105 years), comprises approximately 0.0056% of total natural uranium (Wedepohl, 1978a).
With very long half-lives 238U (4.47 x 109 years), 235U (7.04 x 108 years) and 234U (2.45 x 105 years) are the most commonly encountered uranium isotopes in most rocks. However, some of the longer-lived daughter nuclides (Figure 1), principally 226Ra (half-life; 1599 years), 210Pb (half-life; 22.6 years) and 210Po (half-life; 138.4 days), can also be important naturally-occurring radionuclides. These can be concentrated in some naturally-occurring radioactive material (NORM) wastes from industrial operation: e.g. well and pipeline scale deposits from UK onshore and offshore oil and gas wells (Bassignani et al., 1991; Ceccarello et al., 2004; Read et al., 2004; Garner et al., 2015); mineral processing — in particular, processing ores of titanium, rare earth elements (REEs) and zirconia, phosphate fertilizer production and China clay processing (Beddow et al., 2006).
Radon (222Rn), a gaseous daughter radionuclide produced from the decay of 226Ra within the 238U decay series, is a particularly important natural environmental hazard over uranium-rich rocks in some parts of the UK (Scheib et al., 2013). It may be concentrated in the air of buildings and other places (e.g. underground in caves, tunnels and mines) where ventilation is inadequate or restricted, and is considered to be the largest contributor to radiation exposure in the UK (Watson et al., 2005). Watson et al (op. cit.) estimate that about half of the average annual dose from natural radiation to the UK population comes from radon exposure indoors.
Uranium is a relatively rare element, with an average abundance in the Earth’s crust of between 1 to 3 ppm (Basham and Kemp, 1993; Hazen et al., 2009; Fayek et al., 2011; Cumberland et al. 2016). A generic summary compilation of the distribution of uranium in common rock types is given in Table 1.
|Igneous Rocks||Sedimentary Rocks|
|Syenites and phonolites||0.1–26 ppm||Shales, clays, mudrocks||1–5 ppm|
|Granites and rhyolites||2–50 ppm||Black shales (organic-rich)||2–1250 ppm|
|Intermediate rocks||1–6 ppm||Phosphorite-black shales||≤700 ppm|
|Basalts and other mafic rocks||0.1–1 ppm||Sandstones||0.5–4 ppm|
|Ultramafic||0.001–1 ppm||Limestones, dolomites||<0.1–9 ppm|
|Coals, lignites, peats||1–6000 ppm|
|Metamorphic Rocks||Pure evaporites||<0.1 ppm|
|Medium-grade||<1–5 ppm||Oceanic seawater||0.3–3 ppb|
|High-grade||<1–7 ppm||Groundwater||<0.1–460 ppb|
[based on data from Wedepohl, 1978a; Bowie, 1979; Basham et al., 1989; Ball and Milodowski, 1989;
Basham and Kemp, 1993; Hobday and Galloway, 1999; U.S. Geological Survey, 1997; Cuney, 2010;
Kreuzer et al., 2010; Bowell et al., 2011; Douglas et al. 2011; Alloway, 2013; Cumberland et al., 2016;
Guidez and Gabriel, 2016].
Uranium abundance in igneous rocks
It is a lithophile element i.e. its primary occurrence in igneous rocks is generally in association with rocks containing dominantly light elements (Basham and Kemp, 1993). In general, uranium content increases with magmatic fractionation (Wedepohl, 1978a). Felsic igneous rocks are relatively enriched in uranium: globally, granitic and rhyolitic rocks generally contain between 2 and 15 ppm U, and silicic alkaline rocks often have higher uranium contents (up to 26 ppm U) (e.g. Wedepohl, 1978a; Basham and Kemp, 1993; Cumberland et al., 2016). Some granites can be more uraniferous (Alloway, 2013), with up to 50 ppm U found within some Proterozoic granites in Australia (Kreutzer et al., 2010). Intermediate igneous rocks typically contain between 1 and 6 ppm U. Mafic rocks range from 0.1 to 1 ppm U: average basalt is around 1 ppm U (Alloway, 2013; Cumberland et al., 2016), whereas ultramafic igneous rocks are relatively low in uranium, usually with considerably less than 1 ppm U (Wedepohl, 1978a; Basham and Kemp, 1993).
Uranium abundance in metamorphic rocks
Metamorphic rocks generally contain less uranium than granitic or silicic alkaline igneous rocks. A review by Basham and Kemp (1993) suggests that the uranium concentration in metamorphic rocks is typically between 0.1 to 4 ppm U, and that depletion of uranium takes place with increasing metamorphic grade. However, this is an oversimplification, and as might be expected for rocks derived from a variety of parent materials and under a variety physical-chemical conditions, the variation in uranium content of metamorphic rocks is quite large. Data presented by Wedepohl (1978a) shows a much greater range of compositions from 0.1 to 45 ppm U, with typical values of 1 to 4 ppm U irrespective of metamorphic grade.
Uranium abundance in sedimentary rocks
The concentration of uranium in sedimentary rocks is highly variable. Two of the major factors that influence the uranium content are: (i) the detrital source mineralogy, and; (ii) the redox-chemistry of uranium, which is strongly influenced by the geochemical processes operating during weathering of source rock and sediment transport, within the depositional environment, and during subsequent burial diagenesis. Uranium is redox-sensitive, and although it can exist in 3+, 4+, 5+ and 6+ oxidation states (www.rsc.org/periodic-table/element/92/uranium), only 4+ and 6+ are significant in nature. The occurrence of pentavalent uranium (U5+) has been discovered in the mineral wyartite [CaU5+(UO2)2(CO3)O4(OH).7H2O] (Burns and Finch, 1999), but its occurrence in nature is very rare. Consequently, uranium concentrations in sedimentary rocks can be significantly higher in sedimentary rocks (Table 1) than in the parent igneous rocks (Cumberland et al, 2016). Exceptionally high sedimentary-diagenetic uranium concentrations (>20%) have been produced in the Precambrian, in the Oklo natural reactors, in Gabon (Gauthier-Lafaye et al., 1989). However, these concentrations of uranium are ‘the exception rather than the rule’ in most sedimentary rocks (Table 1):
- sandstones typically contain between 0.5 to 4 ppm U;
- shales and mudrocks typically contain between 1 to 5 ppm U;
- limestones are generally low in uranium — typically about 2 ppm (Wedepohl, 1978a), although some more uraniferous limestones have been reported (e.g. Basham and Kemp, 1993; Milodowski et al., 1989);
- pure evaporites are typically very low in uranium, <0.1 ppm U (Wedepohl, 1978a).
In general, much of the uranium in siliciclastic sedimentary rocks (sandstones, shales, mudrocks) is contained within resistate detrital heavy minerals (e.g. zircon, xenotime, apatite, titanite (sphene), monazite), which occur as trace components, or as inclusions preserved in major detrital minerals such as quartz, feldspars and micas (e.g. Wedepohl, 1978a; Milodowski and Hurst, 1989; Hurst and Milodowski, 1976). In carbonate rocks, the trace concentration uranium is considered to substitute in the lattice in place of calcium.
Organic-rich and phosphatic sediments and sedimentary rocks often host significantly higher concentrations of uranium (Table 1). Phosphorites are often enriched in uranium, with up to 700 ppm reported in some formations (cf. Wedepohl, 1978a; Bowell et al., 2011; Cumberland et al., 2016). Black shales and organic sediments (coals, lignites, peats) display a large variation in uranium content (1 to 6000 ppm: Table 1) with very high concentrations of uranium reported from some formations (e.g. Wedepohl, 1978a; Bowell et al., 2011; Cumberland et al., 2016), including localised concentrations in UK peat deposits (Ball and Milodowski, 1989; Basham et al., 1989; Milodowski et al., 1989).
Uranium host minerals
As mentioned earlier, uranium is a lithophile element: all uranium minerals contain oxygen and it does not occur naturally as the native element nor in combination with sulphur as a sulphide mineral. Over 160 minerals have been identified in which the uranium is essential part of the crystal structure. In addition, uranium can be present as a minor or trace component in a large number of other minerals, incorporated intrinsically by substitution of major ions within the crystal structure (e.g. for Ca2+ in calcium carbonates; titanite and apatite; for Zr4+ in zircon; and rare earth elements (mainly Ce and Y) in rare earth minerals such as monazite and xenotime; niobium-tantalum-titanium minerals, and; iron oxides and oxyhydroxides). Uranyl ions may also be adsorbed on clay minerals, zeolites, oxides and hydroxides iron, manganese and titanium, or may be adsorbed, reduced or form organic-metallic species with organic matter. It is not possible to describe all the uranium-bearing minerals here. Comprehensive lists and accounts of the mineralogy of uranium can be found in Frondel (1958), Heinrich (1958), Wedepohl (1978a), and in reviews by Smith (1984), Finch and Murakami (1999), and Cumberland et al. (2016). Many of these uranium minerals are rare. A brief overview of the uranium principal minerals is given here.
Minerals containing tetravalent u4+
Minerals where uranium is present as a major component in the reduced tetravalent (U4+) state can be divided into three main groups, and the most important minerals are summarised below:
|(i) Simple oxides and silicates||Uraninite-thorite [UO2–ThO2]|
|Coffinite [U (SiO4) 1-x (OH) 4x]|
|Uranothorite-thorite [(U, Th) SiO4]|
|(ii) Complex (multiple) oxides||Brannerite [(U, Ca, Y, Ce, La) (Ti, Fe)2 O6]|
|Davidite [(La, Ce) (Y, U, Fe) (Ti, Fe)20 (O, OH)38]|
|(iii) Phosphate||Ningyoite [(U, Ca, Ce)2 (PO4) 2.1–2H2O]|
Uraninite is the most important and abundant U4+ mineral, and occurs as a primary accessory igneous mineral, and as primary mineral in hydrothermal deposits, and is the main ore mineral of uranium. It is often partially oxidized and commonly referred to as ‘pitchblende’, — a term often used to reflect partially altered and poorly crystalline uraninite.
Coffinite is also a relatively common U4+ mineral and an important uranium ore mineral. It is isostructural; with thorite (ThSiO4) and zircon (ZrSiO4) but unlike these generally magmatic accessory minerals, coffinite is formed at low temperature, either by direct precipitation or often as an alteration product of uraninite. It is nearly always very fine grained and usually poorly crystalline.
Uranothorite is also isostructural with thorite and zircon, often occurring as a primary accessory mineral in alkaline granites, syenites and associated pegmatites (Basham and Kemp, 1993).
Brannerite is the third most important mineral containing U4+ (Basham and Kemp, 1989). It occurs as an igneous or metamorphic accessory mineral, and as a low-temperature phase. Its principal occurrence is in pegmatites, where is may be associated with uraninite. It may also be found in sedimentary rocks, associated with secondary titanium oxide (anatase, rutile) formed as a diagenetic alteration product of primary detrital ilmenite and magnetite (e.g. Milodowski et al., 1989).
Davidite is a complex oxide. It is uncommon and found in rare earth element-rich pegmatites. Ningyoite, named after the type locality in Japan where it was first discovered, is also rare and occurs a low temperature hydrothermal mineral in sedimentary uranium deposits.
Minerals containing hexavalent u6+
There is a great diversity of minerals, where uranium is present as a major component in the oxidised hexavalent (U6+) state. Uranium is present as the uranyl ion ([UO2]2+), often combining with other oxyanion species, including CO32-, PO43-, AsO3-, SO2- and VO43. Complex substitution and replacement can occur within both the cationic and anionic groups, giving rise to a wide range of mineral compositions:
Where: R=P5+, As5+, V5+
A = K+, Na+, H+
B = Ca2+, Ba2+, Mg2+, Fe2+, Pb2+
In addition, many of these minerals are hydrous and contain significant water of crystallisation. Many of these minerals are brightly coloured. They occur as low-temperature secondary minerals, formed within supergene oxidising groundwater and near-surface weathering environments, largely as alteration products of primary uranium mineralisation containing U4+ minerals. However, oxidation of U4+ to much more soluble U6+, coupled with solution and transport within the supergene environment can result in either concentration and redeposition of uranium from a distant large-volume low-level source such as a granite, or to wider dissemination as minor surface coatings from a localised primary uranium concentration such as an orebody (Hazen et al., 2009; Cumberland et al., 2016).
The uranyl phosphates and arsenates represent the most common group of these minerals. They occur in a wide range of geological environments, and exhibit the greatest range of compositions. The autonite (Ca(UO2)2(PO4)2) — meta-autonite (Ca(UO2)2(PO4)2.6H2O), torbernite (Cu[(UO2)(PO4)]2.10–12H2O) — metatorbernite ([Cu(UO2)2(PO4)2·8H2O]), zeunerite (Cu (UO2)2(AsO4)2.8H2O) and troegerite (H2(UO2)2(AsO4)2..8H2O) groups are probably the most widespread of these. This reflects both the natural abundance of P and As in groundwaters around ore deposits and the ready formation of UO2-PO4 and UO2-AsO4 aqueous complexes, and their ability to precipitate in the presence of a variety of cations (Basham and Kemp, 1993). Uranophane is a common uranyl silicate, forming as an oxidative alteration product of primary uranium ores. It has a very variable composition (Cumberland et al., 2016). Hydrated uranyl oxides are also common low-temperature secondary uranium minerals. Schoepite (Ca(H3O)2(UO2)(SiO4)2(H2O)3) is probably the most common of these.
Thorium and its daughter radionuclides
Thorium has only two long-lived natural isotopes, both of which are radioactive (Wedepohl, 1978a). 232Th is the major isotope, with a very long half-life (1.41 x 1010 years), and is the parent of a long radioactive decay series ending with stable 208Pb (Figure 2). The other important natural thorium isotope is 230Th, which is a decay product of 238U (Figure 1). It has a much shorter half-life (7.5 x 104 years) and is generally present in minerals containing uranium (Wedepohl, 1998a). Most of the daughter isotopes of 232Th are very short-lived but 228Ra (half-life 5.75 years) can be an important component in some NORM wastes.
Like uranium, thorium is a relatively rare element, with an average abundance in the Earth’s crust in the range of 6–10 ppm, and more abundant than uranium with an average crustal Th:U ratio of about 3:1 (Adams and Weaver, 1958; Wedepohl, 1978a; Basham and Kemp, 1993; Hazen et al., 2009). Thorium only occurs in the tetravalent oxidation state (Th4+) and, in contrast to highly-soluble hexavalent uranium (U6+), is highly immobile. Consequently, during oxidative alteration, weathering and leaching of primary uranium-thorium minerals, uranium is transported away in solution whereas thorium precipitates locally and is concentrated in residual deposits resulting in geochemical separation (Adams and Weaver, 1958). It forms very few primary minerals and virtually no equivalents of the complex secondary minerals that are characteristic of hexavalent uranium. Typical ranges of thorium concentration for common rock types are summarised in Table 2.
|Igneous Rocks||Sedimentary Rocks|
|Syenites and phonolites||0.7–35 ppm
[typically >10 ppm]
|Shales, clays, mudrocks||10–13 ppm|
|Pelagic clays and
|Granites, rhyolites and
intermediate igneous rocks
|8–56 ppm||Sandstones||1–7 ppm|
|Basalts and other mafic rocks||0.1–4 ppm||Phosphorites||1–5 ppm|
|Ultramafic rocks||<0.1 ppm||Limestones, dolomites||<0.05–3 ppm|
|Highly variable, typically||6–10 ppm||Seawater||0.009 ppb|
|River water||<0.26 ppb|
Thorium abundance in igneous rocks
It is a lithophile element and is predominantly associated with silicic alkaline igneous rocks. Granites and granodiorites may contain around 10 ppm Th, whereas syenites are generally more enriched with up to 35 ppm Th in some cases (Wedepohl, 1978a; Hazen et al., 2009). Basalts and mafic intrusive rocks typically contain between 0.1 to 4 ppm and ultramafic rocks may have even less thorium (Wedepohl, 1978a).
Thorium abundance in sedimentary rocks
The thorium content of sedimentary rocks is highly variable (Wedepohl, 1978a). As discussed above, thorium is highly immobile and tends to be geochemically-separated from mobile uranium during weathering and alteration of primary minerals in igneous parent rocks. Consequently, it is concentrated in resistate detrital heavy minerals such as zircon, monazite, xenotime, apatite etc., or if it is released during weathering then thorium is strongly sorbed onto clays and iron and manganese oxide alteration products. As a result, thorium is often concentrated in residual deposits such as bauxites and heavy mineral placer deposits.
Summary data in Wedepohl (1978a) indicate typical values of around 12 ppm Th for shales and mudrocks; 1 to 7 ppm Th for sandstones; very low values in limestones (because thorium does not enter into the carbonate lattice); 1 to 5 ppm Th in phosphatic rocks, and; >20 ppm in residual deposits such as bauxites and bentonites.
Thorium abundance in metamorphic rocks
The concentration of thorium in metamorphic rocks is highly variable, and is dependent on the thorium content of the original parent igneous or sedimentary rock. Wedepohl (1978a) indicates that thorium concentration can range from <0.1 ppm in marble to >67 ppm in some high-grade feldspathic rocks. However, most metamorphic rocks probably have thorium contents close to the crustal average of between 6–10 ppm Th.
Thorium host minerals
There are only a very small number of primary thorium minerals which contain thorium as an essential component (cf. Wedepohl, 1978a, Basham, 1993). The principal thorium minerals include: thorite (ThSiO4), uranothorite ([Th,U]SiO4), thorianite (ThO2), uranothorianite ([Th,U]O2), thorogummite (Th(SiO4)1-x(OH)4x — analogous to, and isomorphous with, coffinite), and monazite — in particular, the variety cheralite ([Th,Ca,Ce][PO4,SiO4]).
Thorite-uranothorite, thorianite-uranothorianite and monazite (cheralite) occur as primary accessory minerals in alkaline granitic rocks, syenites and associated pegmatites. Monazite has also been found to form as a low-temperature concretionary authigenic mineral in Lower Palaeozoic mudrocks and low-grade metamorphic rocks in the UK and elsewhere (Milodowski and Zalasiewicz, 1991, and references therein). However, authigenic monazites are typically low in thorium. In the UK and Eurpope, they appear to be restricted to rocks of Lower Palaeozoic age (Milodowski and Zalasiewicz, 1981), although recently they have also been found in Triassic rocks from Iran (Alipour-Asli et al., 2012).
Thorogummite typically occurs as a low-temperature secondary mineral, forming from the alteration, weathering or metamictisation of primary thorite or thorium-rich minerals. It is usually fine grained and poorly crystalline (Basham and Kemp, 1993).
Potassium is abundant in the Earth’s crust, with an average crustal concentration of about 2.5% (Wedepohl, 1978b). It has three isotopes, 39K (93.1% isotopic abundance), 40K (0.01% isotopic abundance) and 41K (6.88% isotopic abundance), of which only 40K is radioactive. 40K decays with a half-life of 1250 million years via a combination of beta decay to 40Ca and gamma emission to yield 40Ar. Potassium is a major element in many silicate rocks but may only be present in minor to trace amounts in some sedimentary rocks such as limestones, dolomites and some chemically-precipitated sedimentary rocks. The potassium contents of common rock types is summarised in Table 3.
|Igneous Rocks||Sedimentary Rocks|
|Syenites and phonolites||3–6%||Shales, clays, mudrocks||<0.01–7.1%|
|Granites, rhyolites and
intermediate igneous rocks
|Basalts and other mafic rocks||1–2%||Evaporites:
|Ultramafic rocks||<10 ppm–1%|
|Metamorphic Rocks||Limestones, Dolomites||<0.01–5%|
[av. limestone ~0.3%]
[av. dolomite ~0.6%]
|Dependent on parent rock|
(see igneous and sedimentary)
Potassium abundance in igneous rocks
The abundance and range of concentrations of potassium in common igneous rocks has been collated by Wedepohl (1978b) and is summarised in Table 3.
Potassium is enriched in the more fractionated alkaline silicic rocks and has the lowest concentration in the silica-poor ultramafic rock types. Its concentration primarily reflects the abundance of major potassium silicate minerals, principally: alkali feldspars (orthoclase, sanidine, microcline), micas (biotite, muscovite, phlogopite, paragonite), feldspathoids (nepheline) and alkali-bearing amphiboles:
- Alkali igneous rocks, which include granites, granodiorites, rhyolites, trachytes, typically vary between about 2.5 to 4.5% K;
- Syenites and phonolites are more alkali-rich and have potassium concentrations between 3 to 6% K;
- Intermediate igneous rocks, which include diorites and andesites, typically have potassium concentrations between about 1 to 2% K;
- Mafic igneous rocks, which include, gabbros and basalts, have potassium concentrations typically in the range 0.5 to 1.3% K;
- Ultramafic rocks, which include pyroxenites, anorthosites, dunites, peridotites, and eclogites, typically have very low potassium. However, potassium concentrations vary considerably from <10 ppm K in some dunites and peridotites to about 1% in some anorthosites. An average concentration for ultamafic rocks is about 0.6%.
Potassium abundance in sedimentary rocks
The concentration of potassium in sedimentary rocks is highly variable (Table 3). and dependent on detrital mineralogy, primary chemically-precipitated sedimentary minerals (i.e. evaporite mineralogy), and alteration during sediment burial (diagenesis).
Carbonate rocks and sediments can contain between <0.01 to 5% K. The bulk of the potassium in these materials is essentially contained in the non-carbonate fraction. This largely comprises detrital silicate minerals such as alkali feldspars, micas and clay minerals (particularly potassium-rich clay minerals such as illite, smectite or mixed-layer illite-smectite). Pure limestones and dolomites contains only trace amounts of potassium (Wedepohl, 1978b).
The potassium content of mudrocks (clays, shales, mudstones, siltstones) is largely controlled by the clay mineralogy, with subordinate contribution from K-feldspar (Wedepohl, 1978b). There is usually a strong positive correlation between potassium concentration and clay mineral content. This is also reflected in the wireline gamma-logs of sedimentary sequences, where clay-rich strata normally correlate with an enhanced gamma response (Serra, 1984; Hurst, 1990). The most common and major potassium-bearing clay mineral in mudrocks is illite and clay-grade detrital micas. Less potassic mixed-layer illite-smectite and smectite may also contribute in some clays. Glauconite, which is usually of detrital origin, can also be an important source of potassium in some sedimentary sequences.
The potassium content of sandstones is principally controlled by three main minerals: K-feldspar, mica and glauconite. K-feldspar may be detrital or authigenic in origin. The amount of detrital K-feldspar and mica decreases with increasing sediment maturity. Glauconite is usually formed in situ as authigenic mineral during burial diagenesis. The amount of clay present (which reflects the ‘cleanliness’ or degree of sorting of the sandstone) also influences the potassium content: poorly sorted clay-rich sandstones usually contain more potassium than well-sorted low-clay sandstones.
The potassium content of evaporite rocks is a function of the presence or absence of potassium-rich salts that are precipitated from highly-evolved brines during late-stage extreme evaporation. Pure gypsum, anhydrite and halite contain only minor or trace amounts of potassium. The potassium content of evaporites dominated by these minerals will be influenced largely by the presence of detrital clay minerals. However, late-stage evaporite sequences may include potash deposits formed by the precipitation of potassium salts. There are a large number of potassium salts but the volumetrically most important potassium mineral in evaporites is sylvite (KCl). The mixed salt carnallite (KMgCl3.6(H2O), and the sulphate salt polyhalite (K2Ca2Mg(SO4)4.2H2O), are also important potassium-bearing evaporite minerals.
Potassium abundance in metamorphic rocks
Metamorphic rocks contain a wide variation in potassium concentration. This primarily reflects the nature of the original parent igneous or sedimentary precursor rock. For example, pelitic rocks derived by the metamorphism of mudrocks contain major mica and consequently will contain significant potassium. In contrast, quartzite formed by the metamorphism of a clean quartz-rich sandstone (orthoquartzite) will contain little-or-no potassium.
Distribution of background radioactivity from rocks in the UK
The BGS undertook an assessment of distribution of background γ-radioactivity in the UK in 1983 (Plant et al., 1983), which is summarised in Figure 3. Subsequent assessments for radon potential (Miles et al., 2007; Scheib et al., 2013) provide further information on the distribution of radioactivity in the UK. The distribution of radioactivity closely reflects the underlying bedrock geology (Figure 4).
High background radioactivity is principally associated with large granitic bodies, in particular the evolved potassium-rich alkaline granites, including: the Hercynian southwest England batholith (Dartmoor, Bodmin Moor, Carnmenellis, St Austell and Land’s End granites); Shap and Skiddaw in the Lake District, Cairngorm and Etive in northern Scotland; Caledonian granites of the Southern Uplands of Scotland and northeast England (e.g. Criffell Granodiorite and Cheviot Granite), and the Altanabreac Granite in Sutherland and Caithness, northeast Scotland. These granites contain high concentrations of uranium, thorium and potassium (Plant et al., 1983 and references cited therein). Most of the uranium and thorium in these granitic rocks is hosted within primary igneous accessory minerals such as uraninite/pitchblende, thorite, thorianite, zircon, xenotime, monazite-cheralite, apatite, titanite, allanite and apatite.
High levels of background radioactivity also correspond to the interbedded lacustrine rocks of the Middle Old Red Sandstone (Devonian) of the Orcadian Basin of Caithness, Sutherland, Orkney and Shetland in northeast Scotland. These rocks contain significant uranium closely associated with organic-rich strata, phosphatic fossil-fish beds and localised carbonate-sulphide fracture mineralisation (where minor amounts of uranium minerals are often associated with residual bitumen related to hydrocarbon mobilisation (e.g. Milodowski et al., 1989 and references therein).
The highest levels of total natural radioactivity are associated with localised hydrothermal polymetallic vein mineralisation. The main occurrences include: minor vein mineralisation at the margins of the Criffell Granodiorite on the Solway Coast, at Needle’s Eye, near Dalbeattie (Miller and Taylor, 1965; Gallagher et al., 1976; Basham et al., 1989); Broubster, near Dounreay in Caithness (Gallagher et al., 1976; Ball and Milodowski, 1989; Milodowski et al., 1989), and several other small vein deposits in Caithness and Orkney (Gallagher et al., 1976); and numerous localities in the southwest of England mining region where uranium is concentrated in hydrothermal vein deposits, the most significant of which is at South Terras on the St Austell Granite where uranium was mined commercially in the late 19th and early 20th century (Dines, 1956; Hooker et al., 1989; Read et al., 1991). The principal uranium mineral associated with these vein deposits is uraninite, sometimes associated with coffinite (Basham et al.,1982).
Secondary oxidation, leaching and mobilisation of uranium by percolating groundwater has resulted in the formation of a wide range of secondary low-temperature uranyl minerals associated with many of these deposits. In the case of the Needle’s Eye (Solway Coast) and Broubster (Caithness) uranium mobilised by groundwater from the primary vein mineralisation has been locally concentrated by re-deposition in adjacent organic-rich near-surface sediments (peats and intertidal sediments) to levels in excess of 1000 ppm U (Basham et al., 1989; Ball and Milodowski, 1989; Milodowski et al., 1989).
Moderately-high radioactivity is associated with localised sedimentary facies such as: phosphatic limestone horizons in the Lower Carboniferous Dinanian limestones, mostly in north England; organic-rich marine bands in Namurian and Westphalian mudrocks (e.g. Bowland Shale, Edale Shale); the ironstones and limestones within the Jurassic — i.e. Lias, Inferior Oolite Group (including the Northamptonshire Sand Formation, previously referred to as the Northamptonshire Ironstone) Great Oolite Group and Bridport Sand Formation (Plant et al., 1983; Hodgkinson et al., 2006; Schreib et al., 2013).
The areas of lowest background radioactivity correspond to: the Cretaceous Chalk, Tertiary sedimentary rocks, and unmineralised Lower Carboniferous Limestones in England; granulite-facies Lewisian metamorphic rocks of northwest Scotland, and; areas underlain by mafic and ultramafic rocks in general (e.g. the lizard, Cornwall), Tertiary basalts of northwest Scotland, and mafic and ultramafic rocks of the Grampians and Aberdeenshire).
Other areas of elevated background radioactivity are associated with shale and volcanic lithologies of the Ordovician and Silurian of Wales and the Southern Uplands of Scotland, and the Devonian of southwest England (Figure 3 and Figure 4). Some of these areas are associated with moderate-to-high radon risk (e.g. Environment Agency, 2007; Miles et al., 2007; Scheib et al, 2013), and petrographic analysis indicates that uranium is hosted largely within detrital heavy minerals (zircons etc.), iron-rich clays, goethite alteration products, and phosphatic (apatitic) cements (Hyslop and Pearce, 1999; Hodgkinson et al., 2006 and unpublished BGS data).
Natural background radioactivity at UK nuclear sites
Figures 4 and 5 indicate that, with the exception of Dounreay, Clyde, Rosyth, Hunterston, Torness and Trawsfynydd, most of UK nuclear sites relevant to the responsibility of the NDA are most probably located in areas with low- to moderately-low background radioactivity.
Dounreay is located on the Middle Old Red (Devonian), Caithness Flagstone Group bedrock (Figure 5). These unconformably overly Moine (Late Precambrian) metasedimentary rocks (semipelites and psammites), bodies of dioritic and amphibolitic metamorphosed igneous rocks; intruded by: later Caledonkian (Silurian-Devonian) diorite and granodiorite (Reay Diorite). These crystalline basement rocks outcrop to the south and west of the Dounreay site (Figure 5).
Detailed mineralogical and chemical analyses of these rocks have been reported as part of the UK Nirex site investigations and generic Nirex Safety Assessment Research Programme (NSARP) studies at Dounreay (Milodowski et al., 1991; Hyslop and Milodowski, 1994; Hyslop and Milodowski, 2000; Milodowski et al., 2000).
The Caithness Flagstone Group has a relatively high background radioactivity (Figure 3, and Plant et al., 1983). These rocks are predominantly a succession of lacustrine deposits, comprising a cyclic sequence of feldspathic to subfeldspathic and micaceous sandstones, siltstones, finely-laminated organic-rich shales, and finely-laminated organic-rich limestones sometimes containing abundant phosphatic fossil fish remains (Donovan, 1980). The potassium concentration in the Caithness Flagstone Group rocks at Dounreay ranges from 0.7 to 4.7% K2O (Hyslop and Milodowski, 1994). Within the sandstones, the potassium is hosted largely within detrital K-feldspar and micas, and illite clay matrix. The shales and muddy laminae in the limestones are dominated by detrital chlorite and illite, and therefore illite is probably the main, potassium source. Uranium concentrations in this formation at Dounreay are generally between 1–5 ppm U. However, some horizons are significantly more uraniferous with between 10–25 ppm U (Hyslop and Milodowski, 1994). Fault-rock mineralised by calcite, sulphides and bitumen containing abundant inclusions of uranium silicate (probably coffinite) was encountered within the Caithness Flagstone Group during drilling of the Nirex borehole NDN1 at Dounreay, and found to contain 10–80 ppm U. This produced a strong wireline gamma log response during geophysical logging of the borehole. Thorium is present at concentrations between 5 to 12 ppm Th (Hyslop and Milodowski, 1994). It is present largely in detrital heavy minerals (e.g. monazite). However, traces of authigenic monazite have also been found as authigenic inclusions associated with minor to trace amounts of residual bitumen in the Caithness Flagstone Group (e.g. Milodowski et al., 1989; 1991).
Early BGS mineral exploration studies identified common enrichments of uranium (up to 1500 mg/kg) associated with the phosphatic and black shale horizons throughout the Caithness Flagstone Group of northeast Scotland (Michie et al. 1972). The phosphatic enrichments are typically associated with the fish beds (Donovan’s (1980) lithological association A). Elevated concentrations of lead, zinc, copper, molybdenum and silver are also commonly associated with the uranium enrichments (Michie et al. 1973, Michie, 1970), and zinc and/or molybdenum can be particularly enriched in black shale horizons (Tweedie, 1981). There is strong association between uranium and phosphate content in these rocks (100 ppm U/1% P2O5; Tweedie, 1981), which is consistent with the enhancement of uranium in the fossil fish debris.
A detailed study by Milodowski et al. (1990) of a site of particular enrichment at nearby Broubster to the soth of Dounreay (Michie, 1970) also found uranium largely present within the carbonate lattice of limestone laminae in beds of interlaminated siltstone laminae, limestone and organic laminae (Facies A: Donovan, 1980), and to a lesser extent (although in greater enrichment) in the organic-rich and phosphate-bearing siltstone-mudstone beds (Facies B: Donovan, 1980), where it occurs spatially related to diagenetic pyrite. Additionally, uranium was found associated with early diagenetic hydrocarbons as discrete included minerals, and in calcite-dolomite-barite vein mineralisation containing minor copper and zinc sulphides, uraninite, and residual bituminous hydrocarbon Detailed petrographical studies (Milodowski et al. (1991, 1994; Evans, 1996) observed similar minor diagenetic (matrix) — and fracture-hosted uranium mineralisation associated with residual bitumens elsewhere in the MORS, including in core samples from the Dounreay Shaft area (Milodowski et al., 1991) and from the Nirex Dounreay Borehole NDN1 (Milodowski et al., 1994; Evans, 1996).
Uranium enrichment is also found along the unconformity surface between the MORS and the Moine basement in the Dounreay area. Hyslop and Milodowski (2000) examined the MORS unconformity with the Reay Diorite at Achvarasdal (2.5 km east of Reay) and Borlum House (1 km south of Reay), on granite and amphibolite at Portskerra (~12 km west of Dounreay), and on granite at Baligill (15 km west of Dounreay. They found uranium to be concentrated along the Devonian palaeoweathered horizon (regolith), and hosted largely within fine grained secondary iron and titanium oxides, and accessory secondary light rare earth element (La, Ce, Nd) phosphates. These secondary minerals were associated closely with the weathering and alteration of biotite and amphiboles to chlorite, and the breakdown of primary ilmenite and or titaniferous magnetite to anatase (TiO2) and poorly crystalline secondary Fe-Ti oxide phases. Up to 500 ppm U was found within these secondary phases, although it is unclear whether the uranium is sorbed onto, or if it is incorporated within the crystal structure of, the iron-titanium oxides. Thorium was also found to be present in the same phases.
Detailed autoradiography studies have revealed that uranium mobilisation and enrichment is also encountered on fracture surfaces and within the adjacent altered wallrock matrix in the Caithness Flagstone Group, in association with iron oxyhydroxides formed by near-surface weathering and shallow oxidative groundwater alteration (Milodowski et al., 1990, 1991). The iron oxyhydroxide formation is related to the dissolution and oxidation of ferroan calcite, ferroan dolomite and ankerite cements, and iron sulphides in fracture mineralisation and matrix diagenetic cements. This alteration is associated with alteration in the present-day weathering and shallow groundwater environments.
Detailed mineralogical and petrographical analysis of drillcore from the Nirex Dounreay Borehole NDN1 found minor but significant uranium silicate and uranium-titanium oxide mineralisation, closely associated with calcite and residual bitumen cementing a large fault breccia within a broad silicified zone of Facies A rock in the Caithness Flagstone Group sequence at around 305 m depth. This uranium mineralisation corresponds to the anomalously high gamma response recorded at this depth on the borehole gamma log. The uranium minerals are accompanied by minor amounts of pyrite, galena and barite. Similar uranium silicate and uranium-titanium oxide minerals are found as trace authigenic minerals closely hosted as inclusions within scattered bitumen globules in the matrix of the Caithness Flagstone Group Facies A rocks and occasionally in the more sandstones and siltstones (Milodowski et al., 1994). The same uranium minerals are also found mineralising fossil fish, and accounts for the high degree of radioactivity reported from these fossil fish (Milodowski et al., 1994, and AE Milodowski, unpublished data).
The Clyde site is located on bedrock belonging to the Southern Highland Group (Figure 6). These form part of Dalradian Supergroup, and are probably of Ordovician age. Regionally, they comprise greenschist facies schistose pebbly grits, schistose grits and greywackes, schistose semi-pelites and pelites, together with purple or black phyllites and dark fine-grained limestones. (Roberts, 1977). No specific rock data for uranium, thorium and potassium are available from this site. However, these rock types will be mica (biotitic and/or muscovite) rich, and also likely to contain significant K-feldspar. Consequently, they will be relatively high in potassium. No significant uranium or thorium mineralisation is recorded in this area and uranium and thorium are expected to be generally close to average crustal concentrations.Figure 3 indicates that these rocks moderately radioactive, which would be consistent with most background radioactivity being derived largely from potassium in these mica and feldspar-rich rock types.
The Hunterston site is located on bedrock belonging to the Late Devonian Stratheden Group Group (Figure 7). Regionally, these rocks consist mainly of red-brown sandstones with subordinate conglomerates and mudstones (Browne et al., 2001). No specific rock data for uranium, thorium and potassium are available from this site. However, Figure 3 indicates that these rocks have a relatively high total background radioactivity. Petrographic analyses of this formation from elsewhere in the Midland Valley of Scotland (Milodowski and Rushton, 2008; Monaghan et al., 2012) shows the sandstones are commonly subfeldspathic to sublithic arenites with detrital quartz and minor K-feldspar, albite, muscovite, biotite and chlorite. Mudstones and siltstones are commonly composed of illitic clay with minor quartz, muscovite, biotite and chlorite. Therefore, at least part of the radioactivity will be derived from potassium decay in these potassium-rich minerals. However, it is also possible that the enhanced radioactivity may be related to the presence of phosphatic fossil fish in this formation (Browne et al., 2001).
Rosyth is situated on bedrock belonging to the Lower Carboniferous Strathclyde Group (Figure 8). In the Fyfe region these rocks comprise a sequences of interbedded sandstones with mudstones, mudstones and siltstones with minor limestone, mudstone, and mudstones and siltstone with limestone and dolomite and minor sandstones (Monaghan et al., 2012). The mudrocks in this sequence are organic-rich and include minor oil shales and coals. Nearby to the north, the Strathclyde Group rocks are overlain by, and faulted against, younger Carboniferous strata belonging to the Clackmannan Group. These rocks also comprise cyclical sandstone, mudstone and siltstone with minor limestone, minor coal and sideritic ironstone (Monaghan et al., 2012). Mineralogically, the sandstones are commonly subfeldspathic to sublithic arenites with detrital quartz and minor K-feldspar, albite, muscovite, biotite and chlorite. Mudstones and siltstones are commonly composed of illitic clay with minor quartz, muscovite, biotite and chlorite.
No detailed information for uranium, thorium or potassium are available. Like Hunterston (above) Figure 3 suggests that these Carboniferous rocks have a relatively high total background radioactivity. Some of this radioactivity will be contributed from potassium in detrital K-feldspar, micas and illite, which are abundant in these rocks. However, it is possible that the enhanced background radioactivity could potentially be associated with more organic-rich strata (black shales, coals and oil shales) present in the sequence. These rock types are commonly associated with elevated uranium concentrations (cf. Table 1).
The Torness site is underlain by the Lower Carboniferous Strathclyde Group, which close to the south of the site these rocks overly the Lower Carboniferous Inverclyde Group (Figure 9). In the East Lothian Region the Strathclyde Group comprises cyclical sandstone, siltstone and mudstone with minor coal, seatrock, limestone and ironstone (Monaghan et al., 2012). The underlying Inverclyde Group is dominated by sandstones with some mudstones and pedogenic carbonate rocks (dolostone and calcrete limestone) (Monaghan et al., 2012). Little specific mineralogical data is available but by comparison with rocks of similar age in the Midland Valley to the north (Milodowski and Rushton, 2008; Monaghan et al., 2012), and to the south and from the Southern North Sea (Shaw, 2006), they probably include feldspathic to subfeldspathic sandstones and a clay mineralogy comprised of kaolinite, chlorite and illite.
No detailed information is available for uranium, thorium and potassium in the bedrocks from this site. The total background radioactivity appears to be low to very low. Most of this activity is possibly related to potassium-bearing minerals (K-feldspars and illite).
Chapelcross lies within the Permo-Triassic Carlisle Basin. The site is underlain by the St Bees Sandstone Formation of the Sherwood Sandstone Group (Triassic) (Figure 10). These rocks comprise sporadically micaceous and/or silty, some beds grade up to medium-grained, and intraformational mud clasts are common at some levels (Stone et al., 2012). Thin partings of siltstone, silty mudstone and mudstone may be present.
This area appears to have very low background radiation (Figure 3). No detailed petrological and geochemical data for uranium, thorium and potassium are available for the St Bees Sandstone at this site. However, based on data from elsewhere in northwest England (Strong and Kemp, 1997; Ackhurst et al., 1997; Milodowski et al., 2000; Hyslop et al., 2000) these rocks are likely to be dominated by subfeldspathic sandstones containing minor detrital K-feldspar and mica, and illitic clay present either as matrix clay in poorly-sorted sandstones and mudstone clasts and laminae. Similar sandstones from west Cumbria contain <1 to 4 ppm U, 3 to 9 ppm Th, and 2 to 4% K2O (e.g. Strong and Kemp, 1997; Milodowski et al., 2000; Hyslop et al., 2000). These values are typical of those normally found sandstones globally (Tables 1 to 3, and Wedepohl, 1978a, b). Uranium and thorium are likely to be located principally in detrital heavy minerals — zircon, monazite and apatite. (Milodowski et al., 2000; Hyslop et al., 2000). Fine grained hematitic coatings and hematitic clay matrix material may also contain a minor proportion of the uranium and thorium (Milodowski et al., 2000; Hyslop et al., 2000). The major hosts for potassium with be detrital K-feldspar, mica and illite.
The bedrock at the Sellafield site (Figure 11) is the St Bees Sandstone Formation, which form the lower part of the Triassic Sherwood Sandstone Group (Ackhurst et al., 1997). The area has relatively low total natural radioactivity (Figure 3).
The mineralogy, petrology and geochemistry of these rocks was studied in detail as part of the UK Nirex Limited site investigation programme at Sellafield (1990 to 1997) and within the generic Nirex Safety Assessment Research Programme (NSARP). The sandstones are dominated by subfeldspathic sandstones containing minor detrital K-feldspar and mica, and illitic clay present either as matrix clay in poorly-sorted sandstones and mudstone clasts and laminae (e.g. Strong and Kemp, 1997; Milodowski et al., 2000; Hyslop et al., 2000). They contain <1 to 4 ppm U, 2 to 11 ppm Th, and 2 to 4% K2O (e.g. Strong and Kemp, 1997; Milodowski et al., 2000; Hyslop et al., 2000), which are typical of those normally found sandstones globally (Tables 1 to 3, and Wedepohl, 1978a, b).
The principal mineral hosts for potassium in these rocks are K-feldspar, mica and detrital illite. Uranium and thorium are hosted largely in detrital accessory minerals: zircon (typically several hundred ppm U), monazite (>500 pmm U), and apatite. (up to 50 ppm U) (Milodowski et al., 2000; Hyslop et al., 2000). Uranium is also present in lower concentrations and at variable levels) in secondary sites associated with altered lithic grains (typically several tens of ppm), where is appears to be associated with fine grained hematite (Milodowski et al., 2000).
Calcite vein mineralsation appears to have had little effect on the distribution of uranium in the adjacent wallrock. However, secondary manganese and iron oxyhydroxides, coating the fracture surfaces and penetrating into the adjacent sandstone wallrock of fractures associated with modern groundwater movement, show enhanced levels of uranium (Hyslop et al., 2000). Radium is also concentrated in the secondary manganese-iron oxyhydroxide, which may also be barium-rich (Hyslop et al., 2000). The manganese and iron oxyhydroxide alteration is associated with weathering and oxidation of ferroamanganoan calcite and dolomite vein mineralisation and matrix cements, and alteration of iron-bearing detrital minerals by percolating shallow groundwater (Milodowski et al., 1998).
The Triassic bedrock at Sellafield is covered a thick sequence of till and fluvial-glacial deposits (Ackhurst et al., 1997; McMillan et al., 2004, which may mask the underlying sandstones. These unconsolidated Devensian deposits are, for the large part derived from the underlying local bedrocks. No information is available on the distribution of uranium and thorium in these sediments. However, it is possibly similar to that seen in the St Bees Sandstone Formation.
The Eskmeals site occupies a region of Holocene coastal dunes and interdunes, and shoreface and beach deposits (sand, gravel and boulders) south of the mouth of the River Esk on the margin of the Eastern Irish Sea. These Holocene deposits probably overly a complex sequence of Devensian and older glacigenic deposits that may be up to 70 m thick, which will comprise interbedded tills and glaciofluvial sands, gravels, silts and clays. The bedrock (Figure 12) beneath the superficial deposits will be largely fine- to medium sandstones belonging to the Calder Sandstone Formation — the upper part of the thick sequence of Sherwood Sandstone Group (Triassic) that extends westwards beneath the Irish Sea (Ackhurst et al., 1997; McMillan et al., 2004).
As at Sellafield, the area appears to have a low natural background radioactivity (Figure 3) There are no regional background data for U and Th in soils for Eskmeals. However, BGS GBASE stream sediment data report 2.5 to 2.7 ppm U over glaciofluvial deposits to the south-east of the area, and 2.7 to 3.2 ppm U over the marine deposits that underlie most of the area. Regional data indicates that the natural background concentration of uranium and thorium in Sherwood Sandstone Group bedrock is probably between <1 to 4 ppm U and 2–11 ppm Th. Most of the uranium and thorium will probably reside within resistant trace detrital minerals such as zircon, monazite, apatite and xenotime, although some may also be associated with disseminated iron oxides and sorbed on clay minerals (cf. Hyslop et al., 2000; Milodowski et al., 2000).
The Hartlepool site is underlain by Mercia Mudstone Group and Sherwood Sandstone Group rocks of Triassic age (Figure 13). The area appears to have a moderate degree of natural background radioactivity (Figure 3). The Sherwood Sandstone Group is dominated by feldspathic to subfeldspathic sandstones (similar to those described by Monaghan et al., 2012). The clay mineralogy of the Mercia Mudstone Group in northeast England is dominated by assemblage of major illite or mica and chlorite, variable amounts of corrensite (1:1 mixed-layer chlorite-smectite) (Jeans et al., 2006a). Most of the natural background radioactivity is likely to be contributed by potassium hosted predominantly in the illite-mica-rich Mercia Mudstone Group, and detrital K-feldspar in the Sherwood Sandstone Group (with contributions from illite in more clay-rich sandstone lithologies). Uranium and thorium will be present in trace amounts in accessory detrital phases — principally zircons, monazite, apatite and xenotime.
Further south, enhanced radioactivity may be encounted over the Liassic rocks. The Liassic rocks can give to enhanced radon risk in other parts of the UK but the radon potential map presented by Scheib et al. (2013) suggests this is not problematic in the Hartlepool area.
Heysham is located on the Millstone Grit Group (Namurian). These Carboniferous strata of the Central Pennines of Yorkshire and Lancashire thick, massive sandstone horizons form discrete aquifers separated by intervening mudstones and shales. They include coarse-grained and feldspathic pebbly sandstones. The bedrock in this area has a moderate to high background radioactivity (Figure 3). This probably reflects the radiation contributed by potassium in the feldspathic sandstones, and illite and mica-rich mudstones (cf. Shaw, 2006). Petrographic studies of Namurian sandstones further south showed only very low concentrations of uranium and thorium, hosted predominantly with accessory detrital phases, including zircon, monazite, xenotime, apatite and some organic material (Hyslop and Pearce, 1999).
Interbedded dark mudstones may also be organic-rich, and these could contribute enhanced radioactivity of uranium associated with organic matter (see Table 1).
The Springfields site is located on the Permo-Triassic strata (Figure 15), close to the junction of the Mercia Mudstone Group with the underlying Sherwood Sandstone Group. The area has a moderate natural background level of radioactivity (Figure 3). No detailed background geochemical are readily available for the immediate site. However, petrographic analysis of Sherwood Sandstone Group rocks from the nearby Kirkham borehole (Strong, 1993) show that the sandstone is predominantly subfeldspathic, containing significant K-feldspar with accessory amounts of ilmenite, zircon and apatite, as well as thin mudstones. The clay mineralogy of the sandstone in this area is also illite-dominated (Strong, 1993). Illite is a major component of the Mercia Mudstone Group rocks in this region (Jeans, 2006a). Further south in the Cheshire Basin, both the Sherwood Sandstone Group and the Mercia Mudstone Group are characterised by high potassium and low uranium and thorium (Plant et al., 1999). It seems likely that the geochemistry of these formations in the Springfield area will be similar. Therefore, the moderate natural background radioactivity in this site is due to high levels of potassium in the illitic mudstones of Mercia Mudstone Group and the abundance of K-feldspar in the feldspathic sandstones of the Sherwood Sandstone Group.
The Capenhurst site is located on Lower Triassic Sherwood Sandstone Group Permo-Triassic bedrock at the northerm margin of the Cheshire Basin (Figure 16). This area has a moderate natural background level of radioactivity (Figure 3). Detailed petrographic analysis of Sherwood Sandstone Group rocks show that these sandstones in the Cheshire Basin are predominantly feldspathic to subfeldspathic, containing significant K-feldspar with accessory amounts of ilmenite, zircon, monazite and apatite, as well as thin illitic mudstones and illite clay matrix material (Plant et al., 1999). Illite is a major component of the Mercia Mudstone Group rocks in this region (Jeans, 2006a). Whole-rock geochemical analyses show that they are characterised by high potassium and low uranium and thorium, although trace accessory minerals such as zircon, monazite and apatite can contain uranium in high concentrations (Plant et al., 1999). However, since these phases are only present in trace amounts it is unlikely that they contribute significantly to the background radioactivity. Therefore, it seems likely that the moderate natural background radioactivity in this site is due to high levels of potassium in the Sherwood Sandstone Group.
Wylfa is located on bedrocks consisting of Upper Cambrian, poly-deformed and metamorphosed (greenschist to sub-greenschist facies) chlorite-mica-schists and phyllites (Figure 17). These are predominantly interbedded metamudstones, metasiltstones metasandstones, and red cherts (Phillips, 2011). This area has low to moderate natural background radioactivity (Figure 3), which is largely reflects the abundance of potassium in these mica- and K-feldspar-rich metamorphic strata.
Trawsfynydd rests on Lower Cambrian and Middle Cambrian rocks (Figure 18). These rocks are predominantly metapelites and slatey mudrocks of high (epizonal) metamorphic grade (Merriman, 2006). The rocks are dominated by quartz, and well-crystallised muscovite and chlorite. The area has a moderate to relatively high natural background of radioactivity (Figure 3). Much of this enhanced radioactivity may reflect the abundance of potassium-rich mica in these rocks. However, there is little information on the distribution of uranium and thorium.
Donnington is located on Triassic bedrocks of the Mercia Mudstone Group (Figure 19). This area has a moderate natural radioactivity background (Figure 3). As discussed previously, the Mercia Mudstone Group is characterised by high potassium and low uranium and thorium mudrocks (Plant et al., 1999). Therefore, it seems likely that most of the background radioactivity derived from potassium hosted within these illite-rich mudrocks (Jeans, 2006a).
Sizewell site is located Neogene and younger Quaternary rocks (Figure 20). The area has a very low level of natural background radioactivity. However, there is little readily-available information on the bedrock mineralogy and chemistry, and further investigation is required to evaluate the sources and distribution of any natural radioactive elements.
Bradwell site is located on bedrocks forming part of the Tertiary Thames Group (Figure 21). Regionally, these rocks have a relatively low level of background radioactivity (Figure 3). The bedrock comprises predominantly mudstone, with subordinate muddy sandstones and thin beds of volcanic ash (Huggett and Knox, 2006). The rocks are smectite rich with subordinate illite and mixed-layer illite-smectite (Huggett and Knox, 2006). Although trace amounts of authigenic rare earth phosphate have been identified from the mudstones at the Bradwell site (Bloodworth et al., 1990), it seems likely that much of the low-level background radioactivity is probably derived from potassium hosted by illite. However, little is known about the distribution of uranium and thorium in these rocks and their contribution to background radioactivity.
Amersham is situated of the Cretaceous White Chalk Subgroup (Figure 22). The crop of the White Chalk corresponds to a very low radioactivity background (Figure 3). Essentially, the White Chalk is a very pure calcium carbonate sediment composed largely of calcite with only very minor to trace amounts of clay minerals and detrital components. Consequently, it is expected to have very low concentrations of potassium, uranium and thorium, which is consistent with its low background radioactivity.
The Culham site is located on Lower Greensand Group rocks (Figure 23). These rocks have a moderate to low natural background radioactivity (Figure 3), probably largely because the Lower Greensands contain significant illite, and often glauconite a iron-rich micaceous clay mineral (Jeans, 2006b). Limited mineralogical and chemical analyses reported from drillcore samples recovered from the Lower Greensand Group further south at the Harwell site show the presence of major mica (which includes glauconite) as the dominant clay mineral present, and potassium concentrations of 0.6 to 2% K2O (Wilmot and Morgan, 1982). The concentration of thorium is the same material is between 2 to 6 ppm. No data for uranium is available but the low level of thorium suggests that there is little contribution of uranium from accessory heavy mineral phases.
The Harwell site is located on the Grey Chalk Subgroup, that represents the basal part of the Cretaceous Chalk sequence (Figure 24). This has a very low level back of natural background radioactivity (Figure 3). The geochemistry and mineralogy of samples from Grey Chalk Subgroup at the Harwell site have been described by Wilmot and Morgan (1982). The clay mineralogy is dominated by illite and smectite, but it typically has very low concentrations of potassium (0.6 to 1% K2O) and thorium (1–2 ppm Th). Unfortunately, no data were reported for uranium by Wilmot and Morgan (1982).
Aldermaston is located on bedrocks forming part of the Tertiary Thames Group (Figure 25). This bedrock at this site has a relatively low level of background radioactivity (Figure 3). It comprises predominantly mudstone, with subordinate muddy sandstones and thin beds of volcanic ash (Huggett and Knox, 2006). The Thames Group rocks in this area contain major smectite and illite, with minor chlorite and kaolinite (Huggett and Knox, 2006). Data summarised by Huggett and Knox (2006) suggests that the Thames Group in the Aldermaston area contains significantly more illite than at Bradwell. The natural background radioactivity at this site is probably contributed mainly by potassium hosted illite-rich clay. However, little is known about the distribution of uranium and thorium in these rocks and their contribution to background radioactivity.
Berkley and Oldbury
Berkley and Oldbury sites and situated on Triassic bedrocks within the Worcester Graben (Figures 26 and 27). The natural background radioactivity over these strata in moderate to low (Figure 3), and broadly similar to the background radioactivity encountered over other areas underlain by Mercia Mudstone Group and Sherwood Sandstone Group rocks described previously. It is therefore likely that most of the background radiation is derived from potassium hosted in illite and K-feldspar within similar feldspathic sandstones and illitic mudstones.
The geology of the Cardiff area (Figure 28) includes a wide variety of rocks types ranging from Lower Palaeozoic to Jurassic age. These include mudstones (Lias Group, Mercia Mudstone Group (Upper Triassic), Carboniferous Coal Measures, Devonian strata), sandstones Sherwood Sandstone Group (Triassic), Carboniferous Millstone Grit Group and Coal Measures), and limestone (Dinantian). The area overall has a moderate degree of natural background radioactivity (Figure 3). However, there is little information available on the distribution of uranium, thorium and potassium in these lithologies.
Given the wide range of rock types present the significant variation in uranium, thorium and potassium would be expected, in keeping with the lithological ranges shown in Tables 1 to 3. The more organic-rich or phosphatic horizons within the Coal Measures sequence might be expected to yield significantly higher concentrations of uranium, and consequent higher background radioactivity. Limestone strata may give rise to low background values. Further work is required to understand the controls on the background radioactivity.
Hinkley Point is located on Lias (Lower Jurassic) bedrock (Figure 29). The Lias strata are composed largely of interbedded mudstones and limestones. The area is characterised by low to moderate total background radioactivity (Figure 3).
Some Lias and other Jurassic strata can be responsible for high background radon levels in the UK (Scheib et al., 2013), which would infer enhanced uranium in the bedrock, probably within more phosphatic horizons. However, this does not appear to be the case for the Lias in the Hinkley Point area. Most of the radioactivity is probably contributed potassium in illitic clay in the mudstones. However, little is known about the distribution of uranium and thorium in these rocks and their contribution to background radioactivity.
Winfrith site is located on bedrock belonging to the Bracklesham and Barton Group, within the Hampshire Basin (Figure 30). These rocks are of Eocene age. This area appears to have relatively low background radioactivity (Figure 3).
The Bracklesham beds comprise interbedded to interlaminated clays, silts and mostly fine- or medium-grained sands, locally shelly. Glauconite occurs in the mid part of the sequence. Minor coarse-grained sands, fine gravelly sand, gravel beds, sandstones or ironstone concretions occur in places. The Barton beds are represented by yellow weathering, green-grey clay, with discrete fine-grained sand bands, yellow-pale grey weathering fine-grained sand, green-grey, sandy clay and clayey, silty fine-grained sand. Both units are rich in smectite and illite clay (Huggett and Knox, 2006). Most of the radioactivity is probably contributed by potassium in this illitic clay. However, little is known about the distribution of uranium and thorium in these rocks and their contribution to background radioactivity.
The Portsmouth site is located on Tertiary Thames Group strata, with Bracklesham and Barton Group rocks cropping close by to the south (Figure 31). The area appears to correspond to low natural background radioactivity (Figure 3). As at the Bradwell, Aldermaston and Winfrith sites, these Tertiary strata contain major smectite and illite clay (Huggett and Knox, 2006). Much of the radioactivity is therefore likely to be contributed by potassium from the illite. However, little is known about the distribution of uranium and thorium in these rocks and their contribution to background radioactivity.
The bedrock to the Dungeness site is the lower Cretaceous Wealden Group. In the Wealden Basin these rocks are represented by interbedded thick sandstones, siltstones, mudstones (‘shales’), limestones and clay ironstones of predominantly non-marine facies. The Weald area corresponds to a generally low radioactive background (Figure 3).
The mineralogy and chemistry of samples of Wealden Group rocks from southern England has been described by Kemp et al. (2012). Whole-rock XRD analysis indicates that the samples from the Wealden Group are composed of variable amounts of quartz (25–69%) and phyllosilicates/clay minerals (25–74%) together with a variable range of minor-trace phases including K-feldspar, calcite, dolomite, siderite, anatase, rutile, hematite, pyrite, halite and gypsum. Ironstone horizons are cemented by manganoan-calcian siderite. Typically, the clay assemblages are dominated by mixed-layer illite-smectite (mean 38%) and kaolinite (mean 41%) with minor proportions of illite (mean 18%) and traces of chlorite (mean 2%). These results are similar to other analyses reported elsewhere (Jeans, 2006b). Traces of discrete smectite were identified in some samples. Potassium concentrations range from 0.6 to 3.7% K2O, uranium is present at between 2 to 6 ppm, and thorium ranges from <1 to 19 ppm. The mineralogical distribution of uranium and thorium is unknown but much of the radioactivity can probably be attributed to potassium hosted in illite-smectite clay.
Devonport is located on marine upper Devonian strata (Figure 33) and correspond to a moderate to high degree of background radioactivity (Figure 3). These rocks comprise largely slates, pelites semipelites and psammites of epizontal to anchizonal metamorphic grade, with major K-mica and chlorite (Hillier et al., 2006). Much of the radioactivity is probably attributable to potassium in micas and K-feldspar. However, the mineralogical distribution of uranium and thorium and its contribution to background radioactivity is unknown.
- Wedepohl, K H. (Editor). 1978a. Handbook of Geochemistry: Volume II/5 Elements La(57) to U(92). Springer-Verlag, Berlin, Heidleberg & New York.
- Bourdon, B, Turner, S, Henderson, G M, and Lundstrom, C C. 2003. Chapter 1: Introduction to U-series geochemistry. In: Bourdon, B, Henderson, G M, Lundstrom, C C, and Turner, S P. (Editors), Reviews in Mineralogy & Geochemistry: Volume 52 — Uranium-Series Geochemistry, 1–21. The Mineralogical Society of America, Washington DC, U.S.A.
- Bassignani, A, Di Luise, G, Fenzi, A, and Finazzi, P B. 1991. Radioactive scales in oil and gas production centers. SPE Health, Safety and Environment in Oil and Gas Exploration and Production Conference, 11–14 November, The Hague, Netherlands, SPE-23380-MS (Abstract), 11pp.
- Ceccarello, S, Black, S, Read, D, and Hodson, M E. 2004. Industrial radioactive barite scale: suppression of radium uptake by introduction of competing ions. Minerals Engineering, 17, 323–330.
- Read, D, Rabey, B, Black, S, Glasser, F P, Grigg, C, and Street, A. 2004. Implementation of a strategy for managing radioactive scale in the China Clay industry. Minerals Engineering, 17, 293–304.
- Garner, J, Cairns, J, and Read, D. 2015. NORM in the East Midlands’ oil and gas producing region of the UK. Journal of Environmental Radioactivity, 150, 49–56.
- Beddow, H, Black, S, and Read, D. 2006. Naturally-occurring radioactive material (NORM) from a former phosphoric acid processing plant. Journal of Environmental Radioactivity, 86, 289–312.
- Scheib, C, Appleton, J D, Miles, J C H, and Hodgkinson, E. 2013. Geological controls on radon potential in England. Proceedings of the Geologists Association, 124, 910–928.
- Watson, S J, Jones, A L, Oatway, W B, and Hughes, J S. 2005. Ionising radiation exposure of the UK population: 2005 review. Health Protection Agency Report, HPA-RPD-001, Chilton, Didcot, Oxfordshire. ISBN 0 85951 558 3.
- Basham, I R, and Kemp, S J. 1993. A review of natural uranium and thorium minerals. British Geological Survey Technical Report, WE/93/13. [Report for the Department of the Environment; DoE contract no. PECD 7/9/512; DoE ref. no. DOE/HMIP/RR/94/007.
- Hazen, R M, Ewing, R C, and Sverjensky, D A. 2009. Evolution of uranium and thorium minerals. American Mineralogist, 94, 1293–1311.
- Fayek, M, Horita, J, and Ripley, E M. 2011. The oxygen isotopic composition of uranium minerals: a review. Ore Geology Reviews, 41, 1–21.
- Cumberland, S A, Douglas, G, Grace, K, and Moreau, J W. 2016. Uranium mobility in organic matter-rich sediments: a review of geological and geochemical processes. Earth-Science Reviews, 159, 160–185.
- Bowie, S H U. 1979. The mode of occurrence and distribution of uranium deposits. Proceedings of the Royal Society, London: Mathematical, Physical and Engineering Sciences, 291 (1381), 289–300.
- Basham, I R, Milodowski, A E, Hyslop, E K, and Pearce, J M. 1989. The location of uranium in source rocks and sites of secondary deposition at the Needle’s Eye natural analogue site, Dumfries and Galloway. British Geological Survey Technical Report, WE/89/56 [also as HMIP REPORT, DOE/HMIP/RW/89.091]
- Ball, T K, and Milodowski, A E. 1989. The geological, geochemical, topographical and hydrogeological characteristics of the Broubster natural analogue site, Caithness. British Geological Survey, Technical Report, WE/89/37.
- Hobday, D K, and Galloway, W E. 1999. Groundwater processes and sedimentary uranium deposits. Hydrogeology Journal, 7, 127–138.
- U.S. Geological Survey. 1997. Radioactive elements in coal and fly ash: abundance, forms, and environmental significance. U.S. Geological Survey Factsheet, FS-163-97.
- Cuney, M. 2010. Evolution of uranium fractionation processes through time: driving the secular variation of uranium deposit types. Economic Geology, 105, 553–569.
- Kreuzer, O P, Markwitz, V, Porwal, A K, and McCuaig, T C. 2010. A continent-wide study of Australia’s uranium potential: Part I: GIS-assisted manual prospectively analysis. Ore Geology Reviews, 38, 334–366.
- Bowell, R J, Grogan, J, Hutton-Ashkenny, M, Brough, C, Penman, K, and Sapsford, D J. 2011. Geometallurgy of uranium deposits. Minerals Engineering, 24, 1305–1313.
- Douglas, G B, Butt, C R M, and Gray, D J. 2011. Geology, geochemistry and mineralogy of the lignite-hosted Ambassador palaochannel uranium and multi-element deposit, Gunbarrel Basin, Western Australia. Mineralium Deposita, 46, 761–787.
- Alloway, B J. 2013. Chapter 26 Uranium, In: Alloway, B J. (editor), Heavy Metals in Soils, 656–577, Springer, Netherlands. Cite error: Invalid
<ref>tag; name "Alloway 2013" defined multiple times with different content
- Guidez, J, and Gabriel, S. 2016. Extraction of uranium from seawater: a few facts. EPJ Nuclear Sciences & Technologies, 2, 10pp.
- Kreuzer, O P, Markwitz, V, Porwal, A K, and McCuaig, T C. 2010. A continent-wide study of Australia’s uranium potential: Part I: GIS-assisted manual prospectively analysis. Ore Geology Reviews, 38, 334–366.
- Burns, P C, and Finch, R J. 1999. Wyartite: crystallographic evidence for the first pentavalent-uranium mineral. American Mineralogist, 84, 1456–1460.
- Gauthier-Lafaye, F, Weber, F, and Ohmoto, H. 1989. Natural fission reactors of Oklo. Economic Geology, 84, 2286–2295.
- Milodowski, A E, Basham, I R, Hyslop, E K, and Pearce, J M. 1989. The uranium source-term mineralogy and geochemistry at the Broubster natural analogue site, Caithness. British Geological Survey, Technical Report, WE/89/50. Cite error: Invalid
<ref>tag; name "Milodowski 1989" defined multiple times with different content Cite error: Invalid
<ref>tag; name "Milodowski 1989" defined multiple times with different content
- Frondel, C. 1958. Systematic mineralogy of uranium and thorium. Bulletin of the U.S Geological Survey, 1064, 400pp.
- Heinrich, E W. 1958. Mineralogy and Geology of Radioactive Raw Materials. McGraw-Hill, New York, 654pp.
- Smith, D K. Uranium mineralogy. In Uranium Geochemistry, Mineralogy, Geology, Exploration and Resources, Institute of Mining and Metallurgy, London, pp.43–71.
- Finch, R, and Murakami, T. 1999. Systematics and paragenesis of uranium minerals. Reviews in Mineralogy, 38, 91–180.
- Wedepohl, K H. (Editor). 1978a. Handbook of Geochemistry: Volume II/5 Elements La(57) to U(92). Springer-Verlag, Berlin, Heidleberg & New York.
- Adams, J A S, Weaver, C E. 1958. Thorium-to-uranium ratios a indicators of sedimentary processes — an example of geochemical facies. Bulletin of the American Association of Petroleum Geologists, 42, 387–430.
- Milodowski, A E, and Zalasiewicz, J A. 1991 Redistribution of rare earth elements during diagenesis of turbidite-hemipelagite mudrock sequences of Landover age from Central Wales, In: Morton, A C, Todd, S P, and Haughton, P D. (editors) Developments in Sedimentary Provenance Studies. Geological Society of London, Special Publication, 57, 101–124.
- Alipour-Asli, Mirnejad, A, and Millodowski, A E. 2012. Occurrence and paragenesis of diagenetic monazite in the upper Triassic black shales of the Marvast region, South Yazd, Iran. Mineralogy and Petrology, 103, 197–210.
- Wedepohl, K H. (Editor). 1978b. Handbook of Geochemistry: Volume II/2 Elements Si(14) to V(23). Springer-Verlag, Berlin, Heidleberg & New York.
- Serra, O. 1984. Fundamentals of Well-Log Interpretation 1: The Acquisition of Logging Data. Developments in Petroleum Science, 15A. Elsevier, Amsterdam.
- Hurst, A. 1990. Natural gamma-ray spectroscopy in hydrocarbon-bearing sandstones from the Norwegian Continental Shelf. In: Hurst, A, Lovell, M A, and Morton, A C. (editors), Geological Applications of Wireline Logs. Geological Society of London, Special Publication, 48, 211–222.
- Plant, J, Ostle, D, and Miller, J M. 1983. Natural levels of uranium in Britain — economic and environmental significance. Report, Institute of Geological Sciences, 83/1, 32–39.
- Miles, J C H, Appleton, J D, Rees, D M, Green, B M R, Adlam, K A M, and Myers, A H. 2007. Indicative atlas of radon in England and Wales. Health Protection Agency Report, HPA-RPD-033, 29pp. Health Protection Agency, Chilton, Didcot, Oxfordshire.
- Miller, J M, and Taylor, K. 1965. Uranium mineralisation near Dalbeattie, Kirkudbrightshire. Bulletin of the Geological Survey of Great Britain, 25, 1–18.
- Dines, H G. 1956. The metalliferous mining region of South-West England. Memoirs of the Geological Survey of Great Britain, 2, 541–543.
- Hooker, P J, Ivanovich, M, Milodowski, A E, Ball, T K, Dawes, A, and Read, D. 1989. Uranium migration at the South Terras mine, Cornwall. British Geological Survey Technical Report, WE/89/13 and UK DOE Report. DOE/RW/89.068.
- Read, D, Hooker, P J, Ivanovich, M, and Milodowski, A E. 1991. A natural analogue study of an abandoned uranium mine in Cornwall, England. Radiochimica Acta, 52/53, 349–356.
- Basham, I R, Ball, T K, Beddoe-Stephens, B, Michie, U. McL. 1982. Uranium-bearing accessory minerals in granite fertility: I Methods of identification and quantification; and II Studies of granites from the British Isles. In: Uranium Exploration Methods. Proceedings of a Symposium, Paris, 1982. OECD-NEA/IAEA, Paris, pp.385–397.
- Hodgkinson, E S, Scheib, C, Jones, D G, and Davis, J. 2006. Studies of possible controls on the variability of radon potential of two East Midlands ironstones. British Geological Survey Technical Report IR/06/128, 96pp.
- Scheib, C, Appleton, J D, Miles, J C H, and Hodgkinson, E. 2013. Geological controls on radon potential in England. Proceedings of the Geologists Association, 124, 910–928.
- Environment Agency. 2007. Assessment of naturally-occurring radionuclides in England and Wales. Environment Agency Science Report, SC030283/SR, 78 pp.
- Hyslop, E K, and Pearce, J M. 1999. The mineralogy and petrology of potential radon source rocks from the Liverpool Bay and Lake District areas of the UK. British Geological Survey Technical Report, WG/99/10.
- Hyslop, E K, and Milodowski, A E. 1994. The mineralogy, petrology and geochemistry of the Devonian and Moine rocks of Dounreay Borehole No.1. Nirex Report 639, United Kingdom Nirex Limited, Harwell, Oxfordshire.
- Hyslop, E K, Longworth, G, Chenery, S R, Kemp, S J, and Hards, V L. 2000. Disturbance of uranium-series elements in surface phases and adjacent rock matrix in potential flowing features from Sellafield boreholes RCM2 and RCF3. British Geological Survey Technical Report, WG/96/17.
- Milodowski, A E, Hyslop, E K, Kemp, S J, Gillespie, M R, Chenery, S R, Bland, D J, Prior, S V, Strong, G E, and Wetton, P D. 2000. The mineralogical, petrographical, and uranium and thorium distribution characteristics of Sellafield borehole drillcore samples selected for the Nirex Safety Assessment Research Programme (1993–1994). British Geological Survey, Technical Report, WG/94/34.
- Donovan, R N. 1980. Lacustrine cycles, fish ecology and stratigraphic zonation in the Middle Devonian of Caithness. Scottish Journal of Geology, 16, 35–50.
- Michie, U. McL, and Haynes, L. 1972. Uranium and Zn in stream waters of Caithness. Institute of Geological Sciences Technical Report, WF/AG/70/308.
- Michie, U. McL, Gallagher, M J, and Simpson, A. 1973. Detection of Concealed mineralisation in Northern Scotland. In: Jones, M J.(editor), Geochemical Exploration 1972, Institute of Mining and Metallurgy (London). 117–130.
- Michie, U. McL. 1970. Uranium in the Old Red Sandstone of NW Caithness. Institute of Geological Sciences Technical Report, WF/AG/70/304.
- Tweedie, J R. 1981. The origin of uranium and other metal concentrations in the Helmsdale Granite and the Devonian Sediments of the North-East of Scotland. PhD Thesis, Aberdeen University.
- Evans, D J. 1996. The West Orkney Basin and onshore northern Scotland: an outline of the geology relevant to the hydrocarbon prospectivity. British Geological Survey Technical Report, WA/96/46C.
- Roberts, J L. 1977. Dalradian rocks of Roneath and south-east Cowal. Scottish Journal of Geology, 13, 101–111.
- Browne, M A E, Smith, R A, and Aitken, A M. 2001. A lithostratigraphical framework for the Devonian (Old Red Sandstone) rocks of Scotland south of a line from Fort William to Aberdeen. Version 3. British Geological Survey Research Report, RR/01/04.
- Milodowski, A E, and Rushton, J E. 2008. Mineralogical and porosity characterisation of potential aquifer and seal units for carbon capture and storage methodologies for the CASSEM Project. British Geological Survey Report, CR/08/153.
- Monaghan, A, Ford, J, Milodowski, A, McInroy, D, Pharoah, T, Rushton, J, Browne, M, Cooper, A, Hulbert, A, and Napier, B. 2012. New insights from 3D geological models at analogue CO2 storage sites in Lincolnshire and eastern Scotland, UK. Proceedings of the Yorkshire Geological Society, 59, 53–76.
- Shaw, H. 2006. Clay mineralogy of Carboniferous sandstone reservoirs, onshore and offshore UK. In: Jeans, C V, and Merriman, R J. (editors), Clay Minerals in Onshore and Offshore Strata of the British Isles: Origins & Clay Mineral Stratigraphy, 417−432. Mineralogical Society, London.
- Stone, P, McMillan, A A, Floyd, J D, Barnes, R P, and Phillips, E R. 2012. British Regional Geology: South of Scotland. (Fourth Edition). Keyworth, Nottingham: British Geological Survey.
- Strong, G E, and Kemp, S J. 1997. Off-site Core Characterisation Programme: The Petrographic, Mineralogical and Lithogeochemical Characteristics of Permo-Triassic Rocks from Sellafield Borehole 2. Nirex Report, 734.
- Ackhurst, M C, Chadwick, R A, Holloway, D W, McCormac, M, McMillan, A A, Millward, D, and Young, B. 1997. Geology of the West Cumbria District: Memoir for the 1:50 000 Geological Sheets 28 Whitehaven, 37 Gosforth and 47 Bootle (England and Wales). British Keyworth, Nottingham.
- Milodowski, A E, Gillespie, M R, Naden, J, Fortey, N J, Shepherd, T J, Pearce, J M, and Metcalfe, R. 1998. The petrology and paragenesis of fracture mineralization in the Sellafield area, west Cumbria. Proceedings of the Yorkshire Geological Society, 52, 215–241.
- McMillan, A A, Hamblin, R J O, and Merritt, J W. 2004. An overview of the lithostratigraphical framework for Quaternary and Neogene deposits of Great Britain (Onshore). British Geological Survey Research Report, RR/04/04.
- Jeans, C V. 2006a. Clay mineralogy of Permo-Triassc strata of the British Isles: onshore and offshore. In: Jeans, C.V. and Merriman, R.J. (editors), Clay Minerals in Onshore and Offshore Strata of the British Isles: Origins & Clay Mineral Stratigraphy, 309–354. Mineralogical Society, London.
- Strong, G E. 1993. Diagenesis of Triassic Sherwood Sandstone Group rocks, Preston, Lancashire, UK: a possible evaporitic cement precursor to secondary porosity? In: North, C P, and Prosser, D J. (editors), Characterization of Fluvial and Aeolian Reservoirs, Geological Society, London Special Publication, 73, 279–289.
- Plant, J A, Jones, D G, and Haslam, H W. (editors). 1999. The Cheshire Basin: Basin Evolution, Fluid Movement and Mineral Resources in a Permo-Triassic Rift Setting. British Geological Survey, Keyworth, Nottingham.
- Phillips, E R. 2011. The Geology of Anglesey, North Wales: project scoping study. British Geological Survey Internal Report, IR/09/05. 47pp.
- Hugget, J M, R W O’B. Knox. 2006. Tertiary clay mineralogy of the British Isles. In: Jeans, C V, and Merriman, R J. (editors), Clay Minerals in Onshore and Offshore Strata of the British Isles: Origins & Clay Mineral Stratigraphy, 5–46. Mineralogical Society, London.
- Bloodworth, A H, Milodowski, A E, Inglethorpe, S D J, Cave, M R, and Morgan, D J. 1990. Trace element distributions within samples from argillaceous strata, Bradwell and Fulbeck sites. Nirex Report, NSS/R237.
- Jeans, C V. 2006b. Clay mineralogy of Cretaceous strata of the British Isles. In: Jeans, C.V. and Merriman, R.J. (editors), Clay Minerals in Onshore and Offshore Strata of the British Isles: Origins & Clay Mineral Stratigraphy, 47–150. Mineralogical Society, London.
- Wilmot, R D, and Morgan, D J. 1982. Mineralogical and lithochemical studies of strata beneath the Harwell Research Site. British Geological Survey, Technical Report, ENP 82–13.
- Kemp, S J, Wagner, D, and Ingham, M N. 2012. The mineralogy, surface area and geochemistry of samples from the Wealden Group of southern England. British Geological Survey Internal Report, IR/10/079.
- Hillier, S, Wilson, M J, and Merriman, R J. 2006. Clay mineralogy of the Old Red Sandstone and Devonian sedimentary rocks of Wales, Scotland and England. In: Jeans, C V, and Merriman, R J. (editors), Clay Minerals in Onshore and Offshore Strata of the British Isles: Origins & Clay Mineral Stratigraphy, 433–471. Mineralogical Society, London.