the Creative Commons Attribution 4.0 License.
the Creative Commons Attribution 4.0 License.
Attenuation of beta radiation in granular matrices: implications for trappedcharge dating
Alastair C. Cunningham
JanPieter Buylaert
Andrew S. Murray
Mineral grains within sediment or rock absorb a radiation dose from the decay of radionuclides in the host matrix. For the beta dose component, the estimated dose rate must be adjusted for the attenuation of beta particles within the mineral grains. Standard calculations, originally designed for thermoluminescence dating of pottery, assume that the grain is embedded in a homogenous medium. However, most current applications of trappedcharge dating concern sand or siltsized dosimeters embedded in granular sediment. In such cases, the radionuclide sources are not homogeneous but are localised in discrete grains or held on grain surfaces. We show here that the mean dose rate to dosimeter grains in a granular matrix is dependent on the grainsize distributions of the source grains and of the bulk sediment, in addition to the grain size of the dosimeters. We further argue that U and Th sources are likely to be held primarily on grain surfaces, which causes the dose rate to dosimeter grains to be significantly higher than for sources distributed uniformly throughout grains. For a typical wellsorted medium sand, the beta dose rates derived from surface U and Th sources are higher by ∼ 20 % and ∼ 30 %, respectively, compared to a homogenous distribution of sources. We account for these effects using an expanded model of beta attenuation – including the effect of moisture – and validate the model against Monte Carlo radiation transport simulations within a geometry of packed spheres.
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Trappedcharge dating methods require an estimate of the radiation dose rate to a natural dosimeter, usually embedded in sediment or rock. The dose rate is provided largely through alpha, beta, and gamma radiation arising from the decay of naturally occurring radionuclides (U and Th series and ^{40}K). The decay rates of the radionuclides and the amounts of energy released are relatively well known. By using nuclear data summaries, the measured activity concentrations of a sample can be converted to an infinite matrix (IM) dose rate, i.e. the average dose rate to the bulk sample assuming that the amount of energy absorbed per unit mass equals the amount released. The different components of the dose rate are attenuated by sediment moisture, and require a correction based on the presumed average moisture content during burial. The quantity of interest, however, is the dose rate received by the natural dosimeters in the matrix, which are usually grains of quartz or feldspar. For the beta component, there is an additional grainsizedependent attenuation factor because the range of beta particles in sediment is comparable to the size of the grains. The beta dose rate to the dosimeter grains, ${\dot{D}}_{\mathit{\beta}}$ (Gy ka^{−1}), can then be defined by
where ${\dot{D}}_{\mathit{\beta},\mathrm{IM}}$ is the dry IM beta dose rate (Gy ka^{−1}) and c_{atten} and c_{water} are correction factors for attenuation by grain size and water, respectively. ${\dot{D}}_{\mathit{\beta},\mathrm{internal}}$ (Gy ka^{−1}) is an additional component of the beta dose derived from radionuclides within the dosimeter grain. This formulation implicitly assumes that the contribution to the IM dose rate from the internal activity of any one dosimeter grain is negligible, which is usually true.
Calculation of c_{atten} derives from the selfdose values of the dosimeter grains (Bell, 1979; Mejdahl, 1979; Aitken, 1985, Guérin et al., 2012). For an active grain within a homogenous inactive matrix, the selfdose fraction, φ, is the proportion of the energy emitted by the grain that is selfabsorbed or, equivalently, the beta dose rate to the grain as a proportion of the dose rate to an infinitely large grain. The value of φ is dependent on the grain size and elemental composition, and on the beta energy spectrum (i.e. the radionuclide source). By symmetry, its complement gives the relative attenuation of dose for a nonactive grain in a homogenous, active matrix, hence ${c}_{\mathrm{atten}}=\mathrm{1}\mathit{\phi}$ (see Aitken, 1985, Appendix C therein).
The key assumption in the use of 1−φ is that the matrix surrounding the grain is homogenous at the range of beta radiation. This assumption is likely to be valid in some circumstances, such as for quartz grains imbedded in finegrain pottery – and this was indeed the dominant application of trappedcharge dating in the 1960s and 1970s when the original formulation was developed. However, since the development of Optically Stimulated Luminescence (OSL) dating (Huntley et al., 1985) and especially since the development of singlealiquot OSL protocols (Duller, 1994; Murray and Wintle, 2000), the vast majority of dating applications concern sediment with sandsized or siltsized grains. In such cases, the size of the grains is comparable with the range of beta particles. Beta sources in such sediments are localised – either uniformly distributed throughout the volume of some individual mineral grains, or in secondary mineral coatings formed on grain surfaces – and so their distribution in the matrix is heterogeneous. In such cases it is not clear that the assumption of a homogenous matrix is reasonable (Guérin et al., 2012).
Our aim here is to reassess the beta dose rate calculation for dosimeters in granular sediment, and to propose a model of beta attenuation that is sufficiently simple for routine application. The model (Sect. 2) seeks to achieve this by modifying the 1−φ model that is currently in use, taking account of the variable grainsize distributions of sources, dosimeters, and bulk sediment, and the possibility of sources being held on grain surfaces. As input to the model, Sect. 3 provides revised and extended values of φ for each category of source (K, U, Th) for both wholegrain and surface sources. These φ values take into account a recent revision to the ^{40}K beta spectrum and the effect of etching on the selfdose values of dosimeter grains. In Sect. 4, the simple model of beta attenuation is tested against detailed Monte Carlobased radiation transport simulations with a geometry of closely packed spheres. Section 5 seeks to incorporate the effect of moisture into the revised attenuation model. Section 6 shows empirical evidence of surfaceheld radionuclides in typical samples.
Consider first a single dosimeter grain in a homogenous matrix (Fig. 1a). It is assumed that the grain is too small to have any effect on the matrix activity concentration. An infinitely small grain will receive the IM dose rate, which in this case equals the dose rate in the homogenous matrix. A dosimeter with real mass will receive less than the IM dose rate due to attenuation (i.e. selfshielding). The attenuation is dependent on grain size and is the complement of the selfdose, giving the following equation:
This definition of attenuation has been in common use since Mejdahl (1979). The difficulty arises when we consider a sediment containing more than one grain. Figure 1b and c illustrate a matrix containing many grains within a homogenous source region. The mass of the grains is 50 % of the total mass in both cases, but the size of the grains is different. Let us assume that these grains are inert: they have no radioactive sources. In these scenarios, the IM dose rate equals half the dose rate in the active matrix, and when using the standard approach the dose rate to a dosimeter grain is the same in each case. In reality, however, the presence of other grains in the sediment has an effect on the dose rate to the dosimeter grain. Because the grains are inert, the lowest dose rates in the sediment are found in the middle of those other grains, where the dose is attenuated due to shielding. The dosimeter grain is excluded from these lowdose regions, and so the average dose rate to the dosimeter must be higher than the IM dose rate. The larger the size of those other grains, the stronger the effect.
Accounting for this effect requires the inclusion of a new parameter in the attenuation calculation. This parameter, θ, must describe the relative efficiency of dose absorption for each grain or object in the sediment. It must be dependent on the shape and composition of the grains but be independent of mass; it must also have a value of 1 when averaged over all parts of the sediment so that conservation of energy is maintained. In fact, we already have a parameter that nearly fits this description: 1−φ. Although 1−φ has been defined above as the complement of the selfdose, it can also be thought of as the efficiency of dose absorption in an object relative to a perfect absorber. For example, if a grain has a 1−φ of 0.9, it receives 90 % of the dose to a hypothetical perfect absorber. Of interest here, however, is the efficiency of dose absorption relative to all objects in the matrix. To accomplish this, the 1−φ value appropriate to the dosimeter grain should be normalised to the massweighted average 1−φ for the matrix:
Note that the “matrix” contains everything in the sample, including the dosimeter of interest. For the idealised scenarios of Fig. 1b and c, the attenuation to a dosimeter placed within the matrix would be c_{atten}=θ (in calculating 1−φ_{matrix}, the homogenous source region is a perfect absorber for which $\mathrm{1}\mathit{\phi}=\mathrm{1}$ ). However, in a realistic granular matrix it is not just the dosimeters that exist as discrete grains but also the sources (Fig. 1d). Source grains have their own selfdose, which is dependent on their size and is described by φ_{source}. Only the portion of energy that leaves the source grains ($=\mathrm{1}{\mathit{\phi}}_{\mathrm{source}}$) is available to dosimeters, and all of that energy must be absorbed by the matrix. We can now describe the attenuation coefficient for the portion of the dose derived from wholegrain sources as
where the superscript w indicates that we are considering the φ of a wholegrain source (as opposed to a surface source, discussed below). The relevant φ^{w} values are the massweighted averages for the distribution in question (source, dosimeter, or (entire) matrix). For a grainsize distribution of n bins, the weighted average is
where m is the total mass of the grains in each bin. In practice then, the grainsize distribution of dosimeter grains is usually restricted to a narrow range through grainsize separation in the laboratory. In this case, a weighted average is not necessary for ${\mathit{\phi}}_{\mathrm{dosimeter}}^{\mathrm{w}}$, and instead its value can be drawn directly from Table 1. If the dosimeter grains have been etched, then this should be reflected in ${\mathit{\phi}}_{\mathrm{dosimeter}}^{\mathrm{w}}$ by consulting one of the “etched” columns in Table 1.
With θ written out in full in Eq. (4), it is apparent that if ${\mathit{\phi}}_{\mathrm{source}}^{\mathrm{w}}={\mathit{\phi}}_{\mathrm{matrix}}^{\mathrm{w}}$ then the equation reduces to ${c}_{\mathrm{w}}=\mathrm{1}{\mathit{\phi}}_{\mathrm{dosimeter}}^{\mathrm{w}}$, i.e. the standard definition for a grain in a homogenous matrix. This reduction is valid for the idealised scenario of Fig. 1a; it might also be relevant for some natural sediments if sources are held in whole grains (not on surfaces) and the grainsize distribution of source grains is the same as the bulk sediment, e.g. quartz or feldspar grains in a wellsorted sand with no secondary mineralisation. Note that we only consider average dose rates here, not variations in dose rate from grain to grain; this might be considerable in this example (e.g. Mayya et al., 2006; Cunningham et al., 2012; Guérin et al., 2015).
With slight modification, the φ system can be extended to account for sources that are held on grain surfaces. In this case the selfdose to source grains is substantially reduced (Table 2), meaning that the proportion of energy available to external grains is greater than for wholegrain sources. The variables accounting for attenuation in the dosimeter and the matrix remain unchanged, so we can define c_{s} as the attenuation coefficient for the portion of the dose rate derived from surface sources:
In this case, however, the activity concentration is not uniform across the source grains. If we assume that activity per surface area is constant, it follows that smaller grains have a greater activity concentration due to their greater surfacetovolume ratio. Effectively, the mean grain size of the sources is reduced, which can be accounted for by reweighting φ_{source} according to the surfacetovolume ratio of the grains:
where $\stackrel{\mathrm{\u203e}}{\mathrm{svr}}$ is the surfacetovolume ratio. If we continue to assume grains are spherical, then
Finally, the beta attenuation coefficient for a radionuclide is the weighted average of the two components (wholegrain sources and surface sources):
where p is the proportion of activity held in wholegrain sources.
The preceding discussion of surface sources has concerned those external to the dosimeter grain. If activity is held on all surfaces, there is an additional component of the dose rate that derives from the surface of the dosimeter grain itself. Once again, the activity of the dosimeter grain is influenced by the surfacetovolume ratio of the grain relative to other grains in the sediment:
where ${\dot{D}}_{\mathit{\beta},\mathrm{internal}}^{\mathrm{s}}$ has units of dose rate (e.g. Gy ka^{−1}) and β_{IM} is the infinite matrix dose rate of the radionuclide in the bulk sediment. In practice, only the nuclides in the U and Th chains are likely to be important as surface sources (see Sects. 6 and 7). K may be held on surfaces, e.g. in adhering clay grains, but the selfdose from K surface sources is much smaller than for U and Th (see Table 2).
In the case of Kfeldspar dosimeters, there is a significant internal dose rate derived from the ^{40}K source, which in our notation is
where ${\dot{D}}_{\mathit{\beta},\mathrm{internal}}^{\mathrm{w}}$ also has units of dose rate (e.g. Gy ka^{−1}). ${D}_{\mathit{\beta},\mathrm{IM}}^{\mathrm{grain}}$ is the infinite matrix dose rate of the feldspar grain, and ${\mathit{\phi}}_{\mathrm{dosimeter}}^{\mathrm{w}}$ should be selected from Table 3 (feldspars) using an “etch” column if appropriate.
In Sect. 4 this model is tested against simulations using the Monte Carlo radiation transport code, but first we update and extend tabulated values of φ.
Revised estimates of φ for wholegrain sources (φ^{w}) are given in Table 1, calculated using Monte Carlo radiation transport software MCNP6.2 (Goorley et al., 2012). The model geometry is a spherical quartz grain (density 2.65 g cm^{−3}) embedded in a larger, lowdensity quartz sphere that represents a matrix. Beta electrons are generated uniformly within the quartz grain; energy deposition in the grain is recorded and given here as a proportion of the total energy of the starting particles. The selfdose is defined separately for sources of ^{40}K, the ^{238}U (+^{235}U) series, and the ^{232}Th series. The spectra for the U and Th series are taken from Guérin et al. (2012) and include internal conversion and auger emissions. These spectra were used by Guérin et al. (2012) for equivalent calculations for unetched grains, and the φ^{w} values presented here for unetched U and Th are indistinguishable from theirs. The ^{40}K spectrum used here is the Leutz et al. (1965) curve provided by Cresswell et al. (2018). The Leutz et al. (1965) experimental spectrum has a mean energy of 584 keV, roughly 4 % greater than the spectrum used by Guérin et al. (2012). Cresswell et al. (2018) argue that the higher energy spectrum is a better approximation of the decay transition in ^{40}K, and the result is a modest reduction in selfdose fraction for a K source compared to Guérin et al. (2012) (but a significant increase in the IM dose rate).
Table 1 also shows the selfdose fractions for etched quartz, modelled using concentric spheres of radius 10 and 20 µm less than the grain radius. These estimates use a slightly different definition of φ: they are calculated as the dose (energy per mass) received by the “etched” spheres as a proportion of the IM dose for the grain (as opposed to the usual definition of energy absorbed to energy emitted; the two definitions are equivalent for an unetched grain). The consequence of etching is to increase the selfdose to the grain, because the outer, lowerdose regions have been removed. The relationship is inverted when considering an external dose: for a dosimeter grain in a homogenous matrix source, the effect of etching is to reduce the dose to the grain. However, the effect is relatively small, amounting to a reduction in external dose rate of between ∼ 0.6 % for K and ∼ 2.8 % for Th for a 200 µm grain relative to the IM dose. There is little dependence on grain size, and little difference between a 10 µm etch and 20 µm etch. These results are broadly consistent with the isolated estimates given by Bell (1979) and Brennan (2003).
The selfdose values are also shown for the case of a surface source, φ^{s} (Table 2). Here, the simulations have been repeated but with the source particles generated within 1 µm of the grain boundary. The selfdose to the grains is much lower than for wholegrain sources. The effect of etching is to reduce the selfdose, because the etched regions are located closer to the source. Table 3 shows the φ^{w} values for Kfeldspar (KAlSi_{3}O_{8}) with density of 2.60 g cm^{−3}, required for calculation of the internal dose rate to feldspar grains.
The Balanced Energy Model (BEM) described in Sect. 2 is validated here using Monte Carlo simulations of dose deposition in a simulated matrix consisting of closely packed spherical grains. Three packing configurations have been prepared for discrete grainsize distributions using the PackLSD software (Donev et al., 2005), with each using a total of 5000 spheres with a volumetric packing density of 60 %. The first configuration, “Geometry A” (Fig. 2), uses three grain sizes: 100, 140, and 400 µm diameter, with 50 % of the volume accounted for by the 400 µm grains. This would be an unusual grainsize distribution to observe in nature, and it is used here to test the application of beta attenuation models in extreme cases. Geometries B and C (Fig. 3) are more realistic distributions, corresponding broadly to a loessic silt and a wellsorted medium sand, respectively.
Grains are randomly assigned to be sources, dosimeters, or neither, according to a chosen probability distribution, and simulations were conducted using MCNP6 (Goorley et al., 2012). All grains were given a composition SiO_{2} and density 2.65 g cm^{−3} (note that there is little difference in electron stopping power between the main silicate minerals; e.g. compare Tables 1 and 3 for wholegrain K sources); the remaining space is defined as air with density 1.205 × 10^{−3} g cm^{−3}. Of the six outer boundaries, four are periodic and two are reflective; hence, all energy is conserved within the box geometry. Simulations were run separately for each source (K, U, Th) using the same energy spectra described in Sect. 2. The beta dose (MeV g^{−1}) was recorded in up to 999 dosimeter cells and is expressed here as a proportion of the IM dose rate. A total of four tests are described below using three geometries.
Test A1 uses Geometry A, with sources restricted to 400 µm grains. The total source mass is 50 %, meaning that every 400 µm grain is a source. Simulations are shown separately for K, U, and Th sources, with beta particles initiated homogenously throughout the source grains (“whole grain” sources). The performance of the beta attenuation models is shown in Fig. 2a and b, which plot the estimated beta dose against that observed in the MCNP simulations. The standard model of beta attenuation assumes that the dosimeter grain is embedded in a homogenous matrix and is defined here as 1−φ_{dosimeter}. In this test, the standard model overestimates the dose to dosimeter grains by 6 %–11 %. Source grains are large and have a large selfdose, hence there is less energy available to be deposited in dosimeter grains. The Balanced Energy Model takes this into account and gives accurate estimates of attenuation for each source (Fig. 2b).
Test A2 uses Geometry A, with wholegrain sources restricted to 100 µm grains. The total mass of sources is 6.5 %, corresponding to 918 out of the 3837 100 µm grains. In this case, the selfdose to the source grains is small, yet a large proportion of the mass is comprised of 400 µm grains. The dosimeter grains (100 and 140 µm), which are smaller than the sediment average, receive a largerthanaverage dose. Note that when the sources are ^{40}K the attenuation is greater than 1, meaning that the dose received by the dosimeters is greater than the IM beta dose for the bulk sediment (this is balanced by the lowerthanaverage dose received by the 400 µm grains). The 1−φ_{dosimeter} model underestimates the attenuation by 6 %–10 % depending on the source (Fig. 2c), while the BEM is consistent with the Monte Carlo simulations (Fig. 2d).
Test B1 uses Geometry B, which has a grainsize distribution broadly corresponding to a coarse silt. Source grains comprise 19 % of the total and have the same size distribution as the matrix. Separate simulations have been run for wholegrain and surface sources. Dosimeter grains are 20 and 40 µm in diameter. In the case of wholegrain sources, the attenuation estimated by 1−φ_{dosimeter} and the BEM are identical and correspond closely to the Monte Carlo simulation (Fig. 3a and b). The two models are not equivalent in the case of surface sources for three reasons. Firstly, the selfdose of the sources is reduced because the sources are not generated in the centre of the grain. Secondly, the effective mean grain size of the sources is also reduced because of the greater surfacetovolume ratio of smaller grains. Thirdly, the dosimeter grains receive a selfdose from sources held on their surface. For surface sources of U and Th, the 1−φ_{dosimeter} model of attenuation underestimates the simulated beta dose by ∼ 7 %. In contrast, the BEM remains accurate.
Test C1 uses Geometry C, corresponding to a wellsorted sand with mean grain size of 250 µm. Again, source grains (19 %) have the same grainsize distribution as the matrix. The simulated attenuation is shown for 200 µm dosimeters (Fig. 3c and d), for wholegrain and surface sources. For grain sizes of 250 µm there is a significant selfdose to source grains (see Table 1), which is much reduced if sources are located on grain surfaces (see Table 2). As such, the energy available to dosimeters is greater when sources are located on grain surfaces. In addition, there is a significant selfdose to dosimeter grains from surfaceheld sources. These effects are not accounted for by the 1−φ_{dosimeter} model of attenuation, leading to an underestimate of simulated beta dose by 9 %, 17 %, and 23 %, for K, U, and Th sources, respectively. The effect is accounted for in the BEM, which gives accurate estimates of attenuation.
Moisture in sediment absorbs radiation. Energy thus absorbed is unavailable to the sediment, reducing the dose rate received by dosimeter grains. The strength of the required correction is largely defined by the average mass of water during the burial period. For beta radiation, the coefficient of attenuation by water, c_{water}, is derived from Zimmerman (1971):
where W is the watercontent fraction, expressed as [mass of water $/$ mass of dry sediment]. The dimensionless parameter x describes the degree to which water is more effective at absorbing beta radiation than the bulk sediment. The value of x has been estimated as 1.25 (Zimmerman, 1971) or 1.19 (Aitken and Xie, 1990) using the ratios of the stopping powers of Al (Zimmerman) or SiO_{2} (Aitken and Xie) compared to water over the relevant range of beta energy. Values close to 1.20 have been confirmed using Monte Carlo radiation software (Nathan and Mauz, 2008; Guérin et al., 2012). However, these estimates effectively assume that the sediment is a homogenous mixture of elements. Guérin et al. (2012) have questioned the accuracy of x for granular sediment, noting that variations in pore size and moisture content may lead to a different value for x.
Using the framework of the BEM, we can attempt a fuller explanation of the role of water in beta attenuation. Noting again that x is a ratio, we need to define the efficiency of dose absorption in pore water and in the dry matrix. In fact, the latter has already been defined in Sect. 2 as 1−φ_{matrix}. This value is calculated as the weighted average of the 1−φ^{w} values for all grains in the matrix. For finegrained matrices, the selfdose of the grains is very small, and thus 1−φ_{matrix} ∼ 1. As the grain size increases, the value of 1−φ_{matrix} becomes significantly less than 1. To calculate x, we need to include a similar parameter for the efficiency of dose absorption by pore water so that
where ${\left[\mathrm{1}{\mathit{\phi}}_{\mathrm{water}}\right]}_{\mathrm{eff}}$ is the effective 1−φ of the pore water. The evaluation of ${\left[\mathrm{1}{\mathit{\phi}}_{\mathrm{water}}\right]}_{\mathrm{eff}}$ is more difficult, but there are some constraints on its value. First, we can recognise that pore water attenuates beta particles, and so it is a nonperfect absorber of radiation definable by 1−φ_{water}, i.e. dependent on the shape and density of the pore water. We must also account for the difference in elemental stopping power between the dry matrix and water, previously assessed as ∼ 1.20. We might expect that ${\left[\mathrm{1}{\mathit{\phi}}_{\mathrm{water}}\right]}_{\mathrm{eff}}\sim \mathrm{1.2}\left(\mathrm{1}{\mathit{\phi}}_{\mathrm{water}}\right)$. In the limiting case of a homogenous matrix, where both 1−φ_{matrix} and 1−φ_{water} equal 1, then x=1.20. As the grain size (and pore size) increases, 1−φ_{matrix} decreases faster than 1−φ_{water} (because the density of water is always much less than mineral grains). In consequence, the ratio x increases with grain size. In contrast, when the water content increases then so does its selfdose, thus 1−φ_{water} decreases and x decreases. However, for sandy and silty sediments, it is likely that the selfdose of the water is very close to zero even for saturated sediment. In practice then, a reasonable approximation for x is
The application of this model can be seen in Fig. 4, in which Monte Carlo simulations have been repeated using geometry C1 (wellsorted sand, mean = 250 µm) with pore space occupied by water at densities corresponding to 1 %–30 % W. The external beta dose to 200 µm grains is shown to decrease as W increases, at a faster rate than predicted using x = 1.20. When x is instead estimated from Eq. (14), the predicted dose is much closer to that observed from the simulation results. The use of Eq. (14) introduces no error for K sources and only small errors in the case of U and Th. Firstly, for U and Th sources the pore water in this simulation has a nonnegligible selfdose, and thus Eq. (14) leads to a slight overestimation of x (Fig. 4b–c). In contrast, Eq. (14) slightly underestimates x for U and Th sources when they are held on grain surfaces (Fig. 4e–f). This is more difficult to explain but might be caused by differences in the beta energy spectra between wholegrain and surface sources (significant proportions U and Th series beta energy is carried by very lowenergy electrons, which would never leave a wholegrain source).
An alternative to Eq. (14) is to estimate x using a Monte Carlo simulation with a representative grainsize distribution. Table 4 provides estimates of x for four grain geometries, each built from a 1000grain packed cube, with 60 % volumetric packing density. The grainsize distributions represent wellsorted silt or sand, with mean grain size ranging from 50 to 300 µm, including the “silt” and “sand” distributions used in Sect. 2. Beta particles are simulated within the grains or on grain surfaces, with the grains once again specified to be SiO_{2} with density of 2.65 g cm^{−3}. Pore water is homogenous, with a density set to reflect the chosen water content from 1 %–30 %. The value of x is defined as the dose to water divided by the (average) dose of the grains. For this calculation, only the external beta dose is considered (i.e. 1−φ_{source}) because the internal dose rates (in both sources and dosimeters) are not affected by water. The x values listed in Table 4 have several significant features. First, it is clear that x is always greater than 1.20 for granular matrices. For siltsized matrices, x values are only slightly greater than 1.20 and show little dependence on the water content or radionuclide source. For sandsized matrices, the differences in x are much starker, particularly for surfaceheld sources of U and Th. For the coarsest simulation (mean grain size of 305 µm), x ranges from 1.34 (K sources with 30 % W) to 2.37 (surfaceheld Th and 1 % W). However, the most extreme values of x occur when the water content is very low (e.g. 1 %), in which case the attenuation calculation is not very sensitive to x. In practice, selecting x from a range of simulated values (Table 4) offers little improvement when compared with the simplicity of Eq. (14), even when (as here) the grainsize distribution is known exactly (see Fig. 4).
The watercontent correction can be achieved using Eq. (12), after either selecting an appropriate value of x for each radionuclide from Table 4 or using the simple approximation in Eq. (14). However, there is an alternative formulation to obtain the same result, which we note here to show the integration of the watercontent correction within the BEM. Via Eqs. (3)–(5), we explained that beta attenuation to dosimeter grains depends on how the efficiency of dose absorption in the dosimeters (1−φ_{dosimeter}) compares to the efficiency of all absorbers in the (dry) matrix (1−φ_{matrix}). In the wet matrix, pore water functions as an additional absorber and could be included in the denominator of Eq. (4). For example, when considering the wholegrain sources of a radionuclide, the attenuation coefficient to dosimeters in the wet matrix, c_{w,wet} would be
which is similar to Eq. (4) but with a mass correction for the water $(\mathrm{1}/\mathrm{1}+W)$, and the 1−φ of the wet matrix in the denominator. The latter is defined by including ${\left[\mathrm{1}{\mathit{\phi}}_{\mathrm{water}}\right]}_{\mathrm{eff}}$ in the weighted average of 1−φ values of all objects in the matrix (Eq. 5). This can be written explicitly as
noting again that (to a first approximation) ${\left[\mathrm{1}{\mathit{\phi}}_{\mathrm{water}}\right]}_{\mathrm{eff}}\sim \mathrm{1.20}$ for siltsized and sandsized matrices. This formulation is exactly equivalent to Eqs. (12) and (13).
The Balanced Energy Model seeks to account for the size distribution of sources, dosimeters, and the matrix, as well as for the location of radionuclides in the source grain. It was observed, however, that the model simplifies to 1−φ_{dosimeter} when two conditions are met: (1) the source grainsize distribution is the same as the matrix, and (2) radionuclides are distributed homogenously within source grains. These conditions can be tested by measuring the radionuclide concentrations for different grainsize fractions of a sample. If sources are held on grain surfaces, the radionuclide concentrations would be proportional to surfacetovolume ratio (e.g. Olley, 1994). Similarly, any difference in the grainsize distributions of source and sediment would show up as a grainsize dependence in radionuclide concentrations. Therefore, if conditions (1) and (2) are met, the radionuclide concentrations would be independent of grain size and the Balanced Energy Model could be simplified to 1−φ_{dosimeter}.
The dependence of radionuclide concentration on grain size is tested here for selected samples from sandsized and siltsized sediments:

Sample 178108, a coarse sand from Pleistocene fluvial terrace of the Tejo River, Portugal;

Sample 178110, a fine sand from coastal aeolianite (rich in quartz and containing some carbonate bioclasts and pedogenic nodules), Oitavos region, Portugal;

Sample 178113, a late Pleistocene loess from Dunaszekcső, Hungary (Újvári et al., 2018);

Sample 191597, a late Holocene loess from Adventdalen, Svalbard (Gilbert et al., 2018).
Samples were separated into grainsize fractions by wet sieving and Stokes settling and then ashed, ground, and embedded in wax casts in preparation for gamma spectrometry. Measurements were performed on a number of HpGe gamma spectrometers at the DTU laboratory, following the procedures described in Murray et al. (1987, 2018): briefly, the ^{40}K gamma emission is measured directly, ^{226}Ra is defined by the gamma emissions of its progeny ^{214}Pb and ^{214}Bi and forms the most precise definition of U series activity (we make no judgement here on the state of disequilibrium in nature), and ^{232}Th is defined by the gamma emissions of its progeny ^{228}Ac and ^{212}Bi, assuming secular equilibrium.
Activity concentrations are plotted in Fig. 5 as a function of the surfacetovolume ratio of the grains in each fraction. The grainsize fractions are indicated on the secondary x axis. For sandsized samples (Fig. 5a–f) there is a clear difference between the trends for ^{40}K and for ^{226}Ra and ^{232}Th. For ^{226}Ra and ^{232}Th, the concentrations are proportional to the surfacetovolume ratio when grain sizes are less than 250 µm. This proportionality is lost for the larger grainsize fractions. The trend is a strong indication that U and Th sources are held on grain surfaces. The nonproportionality in larger fractions could reflect the carbonate component: fragments of shell or pedogenic carbonate nodules are generally larger than the silicate grains and may have U and Th sources that are independent of grain size. In the case of ^{40}K, there is no evidence of proportionality with surfacetovolume ratio, and for sample 178108 there is little dependence on grain size. There is a peak in the ^{40}K content at the most dominant grainsize fraction, which is more pronounced for sample 178110. The association of peak location with dominant grain size suggests that the ^{40}K source lies in the silicate fraction – presumably Kfeldspar – with the concentrations diluted by nonsilicate minerals (carbonates) at the extremes of the grainsize distribution. The trends are broadly similar for the loess samples (Fig. 5g–l). The dominant grainsize fraction of these samples is in the 20–90 µm range. In this range, the ^{226}Ra and ^{232}Th activity concentrations are proportional to surfacetovolume ratio; the relationship is largely absent for ^{40}K. For the loess sample 191597 (Fig. 5j–l), there is also an increase in activity towards larger grainsize fractions; these fractions are very minor by quantity and presumably represent a locally sourced nonloessic component of the soil.
Gamma spectrometry measurements on grainsize fractions (Sect. 6) show that, for samples considered here, activity concentrations of ^{226}Ra and ^{232}Th are largely proportional to surfacetovolume ratio of the grains. These observations are in line with previous findings (e.g. Megumi et al., 1982; Olley, 1994) and readily explained by the patterns of mobility exhibited by the different elements. The igneous sources of U and Th lie in granites and pegmatites. U and Th can form the major or minor component of accessory minerals (zircon, monazite) but are also found in significant concentrations adsorbed to crystal or grain boundaries and as trace elements in the main silicate minerals (Gascoyne, 1992). Under oxidising conditions at the Earth's surface, the weathering of igneous rock leads to the mobilisation of U and Th. Uranium is oxidised into its stable 6+ state, forming the soluble uranyl ion, and also readily adheres to particulates. Thorium is relatively insoluble but is significantly mobilised as colloids or adsorbed on grain surfaces. In soils and sediments, U, Th, and Ra are likely to be bound to iron and manganese oxide crusts, deposited through coprecipitation or ion exchange. Mobilisation processes are influenced by properties of the mineral host (e.g. surface area), the solution (e.g. pH, salinity), and the chemical properties of the species (Chabaux et al., 2003; Carvalho et al., 2014). Note also that the chemical differences between U, Th, and Ra make it unlikely that the surfacebound radionuclides are in secular equilibrium (for example, the excess of ^{226}Ra observed by Olley, 1994).
The presence of radionuclides on grain surfaces has an influence on the average beta dose rate to dosimeter grains. Source grains have a selfdose, which is dependent on the size of the grain, and that portion of their total emitted energy is therefore unavailable to dosimeter grains. When radionuclides are held on the surface of source grains, the selfdose is reduced compared to a wholegrain source, leading to an increase in the dose available to dosimeters. In Sect. 3, the calculation of beta dose rates has been revised by expanding the φ system, with wholegrain and surface sources accounted for separately. The model requires an estimate, for each radionuclide category, of the proportion of activity that is held in wholegrain sources (p in Eq. 9). In the case of ^{40}K, this should normally equal 1 because it is likely that for most sediments the majority of the K is held in the primary mineral form (Kfeldspar). The choice is more difficult in the case of U and Th, because both wholegrain and surface sources are possible. We suspect that surface sources predominate for most dating applications (so p = 0), as is the case for the samples tested in Sect. 6. However, for some sediments the U and Th sources are located in resistant minerals – principally zircon and monazite. These minerals can become concentrated as placer deposits in beach sediment, most often in tropical regions where rates of erosion are high (Gascoyne, 1992). In such cases, concentrations of U and Th would correlate with heavy minerals and associated elements (e.g. Murray and Mohanti, 2006).
The increase in dose rate due to surfaceheld sources is most significant for sandsized sediments. In model C1, for example, the U and Th beta dose rates are increased by ∼ 20 % and ∼ 30 %, respectively, compared to wholegrain sources of the same size (see Sect. 4). For siltsized sediments, the increase is roughly 7 % for U and Th, although likely to be sensitive to dosimeter grain size. At present, trappedcharge dating methods are most commonly applied to sandy or silty sediments, hence the BEM has immediate relevance to dating applications. Samples with high (U + Th) : K ratios will be most affected: the U and Th radionuclides are most likely to be held on surfaces, and the consequences of this are also more severe than for ^{40}K. However, the estimated mean energy of ^{40}K has recently been revised upwards (Cresswell et al., 2018). Taken together, the BEM and the Cresswell et al. (2018) conversion factors will tend to increase the estimated dry beta dose rates by roughly 10 %–20 % for sandy sediments, and ∼ 6 % for silty sediments, compared to current practice. However, current practice also underestimates the attenuation of the beta dose rate by water, particularly if sources are held on grain surfaces. The parameter x (describing the degree to which water is a more effective absorber of dose than the dry matrix) is not a constant but is dependent on the grainsize distribution and somewhat dependent on the water content. The dependence of x on grain size, and the increased dose rate from surfaceheld sources, have both been observed in a previous simulation study (Guerin et al., 2012). The BEM is able to go further: it provides an explanatory model for the effects by using 1−φ as a parameter to describe the efficiency of dose absorption, and it provides a means of accounting for the effects that is simple enough for routine analysis (see Supplement).
We have focused discussion on the way surfaceheld sources alter the attenuation calculation, but the BEM also departs from 1−φ_{dosimeter} when the grainsize distribution of sources differs from that of the bulk matrix. This might occur in sediment with a complex provenance and/or a broad grainsize distribution: for example, a sand with a loessic component, or a coastal sediment containing large shell fragments. The BEM provides a framework for the beta dose rate calculation in such cases; all that is needed is the grainsize distributions of source and sediment, and the average φ value for each distribution. The φ value for a shell, for example, can be obtained relatively simply with radiation transport codes – far simpler than building a full geometry for a mixed sediment (cf. Cunningham et al., 2011; Cunningham, 2016). Finally, we should note that the average beta dose rate is unaffected by the number of source grains (although the dispersion certainly is).
For a single grain in a homogenous matrix, grainsize attenuation of the beta dose rate is accurately defined by 1−φ_{dosimeter}. In a granular matrix, 1−φ_{dosimeter} is only accurate on average if the size distribution of source grains is the same as the bulk matrix. This assumption fails, for example, if radionuclides are held on grain surfaces, which is likely in the case of the U and Th series. The Balanced Energy Model of beta attenuation, described here, modifies and extends the φ system so that it is applicable to granular sediment. The BEM has been successfully tested against radiation transport modelling and is able to account for surfaceheld sources, for differences in the grainsize distributions of source and sediment, and for the grainsize dependence of the watercontent correction. Its use is likely to improve the accuracy of beta dose rate estimates for dating applications.
A spreadsheet implementation of the Balanced Energy Model is included in the Supplement. All data in this paper is given in the figures, tables, or Supplement.
The supplement related to this article is available online at: https://doi.org/10.5194/gchron45172022supplement.
JPB and ASM initiated and guided the project. ACC designed the model, conducted simulations and measurements, and prepared the manuscript.
The contact author has declared that none of the authors has any competing interests.
Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
Our thanks to Pedro Cunha, Gábor Újvári, and Christian Rasmussen for providing samples. We are very grateful to Guillaume Guérin and Svenja Riedesel for their thoughtful reviews of the manuscript and to Barbara Mauz for commenting on the preprint.
This research has been supported by the European Research Council, H2020 European Research Council (RELOS, grant no. 639904).
This paper was edited by Julie Durcan and reviewed by Guillaume Guérin and Svenja Riedesel.
Aitken, M. J.: Thermoluminescence dating, Academic Press, ISBN13: 9780120463817, 1985.
Aitken, M. J. and Xie, J.: Moisture correction for annual gamma dose, AncientTL, 8, 6–9, 1990.
Bell, W. T.: Attenuation Factors for the Absorbed Radiation Dose in Quartz Inclusions for Thermoluminescence Dating, AncientTL, 2–13, 1979.
Brennan, B. J.: Beta doses to spherical grains, Radiat. Meas., 37, 299–303, https://doi.org/10.1016/S13504487(03)000118, 2003.
Carvalho, F., Chambers, D., Fernandes, S., Fesenko, S., Goulet, R., Howard, B., Kim, C. K., Martin, P., Moore, W. S., and Phaneuf, M.: The environmental behaviour of radium: revised edition, International Atomic Energy Agency,ISBN13: 9789201433107, 2014.
Chabaux, F., Riotte, J., and Dequincey, O.: UThRa fractionation during weathering and river transport, in: Uraniumseries geochemistry, edited by: Bourdon, B., Henderson, G. M., Lundstom, C. C., and Turner, S. P., Mineralogical Society of America, Washington, DC, USA, TS14 ISBN13: 9780939950645, 2003.
Cresswell, A. J., Carter, J., and Sanderson, D. C. W.: Dose rate conversion parameters: Assessment of nuclear data, Radiat. Meas., 120, 195–201, https://doi.org/10.1016/j.radmeas.2018.02.007, 2018.
Cunningham, A. C.: External beta dose rates to mineral grains in shellrich sediment, Ancient TL, 34, 1–5, 2016.
Cunningham, A. C., Bakker, M. A. J., van Heteren, S., van der Valk, B., van der Spek, A. J. F., Schaart, D. R., and Wallinga, J.: Extracting stormsurge data from coastal dunes for improved assessment of flood risk, Geology, 39, 1063–1066, https://doi.org/10.1130/G32244.1, 2011.
Cunningham, A. C., DeVries, D. J., and Schaart, D. R.: Experimental and computational simulation of betadose heterogeneity in sediment, Radiat. Meas., 47, 1060–1067, https://doi.org/10.1016/j.radmeas.2012.08.009, 2012.
Donev, A., Torquato, S., and Stillinger, F. H.: Neighbor list collisiondriven molecular dynamics simulation for nonspherical hard particles. I. Algorithmic details, J. Comput. Phys, 202, 737–764, 2005.
Duller, G. A. T.: Luminescence dating of sediments using single aliquots: New procedures, Quaternary Sci. Rev., 13, 149–156, https://doi.org/10.1016/02773791(94)900418, 1994.
Gascoyne, M.: Geochemistry of the actinides and their daughters, in: Uraniumseries disequilibrium: applications to earth, marine, and environmental sciences, edited by: Ivanovich, M. and Harmon, R. S., Oxford University Press, Oxford, ISBN: 9780198542780, 1992.
Gilbert, G. L., O'Neill, H. B., Nemec, W., Thiel, C., Christiansen, H. H., and Buylaert, J.P.: Late Quaternary sedimentation and permafrost development in a Svalbard fjordvalley, Norwegian high Arctic, Sedimentology, 65, 2531–2558, https://doi.org/10.1111/sed.12476, 2018.
Goorley, T., James, M., Booth, T., Brown, F., Bull, J., Cox, L. J., Durkee, J., Elson, J., Fensin, M., and Forster, R. A.: Initial MCNP6 release overview, Nucl. Technol., 180, 298–315, 2012.
Guérin, G., Mercier, N., Nathan, R., Adamiec, G., and Lefrais, Y.: On the use of the infinite matrix assumption and associated concepts: a critical review, Radiat. Meas., 47, 778–785, 2012.
Guérin, G., Jain, M., Thomsen, K. J., Murray, A. S., and Mercier, N.: Modelling dose rate to single grains of quartz in wellsorted sand samples: The dispersion arising from the presence of potassium feldspars and implications for single grain OSL dating, Quat. Geochronol., 27, 52–65, https://doi.org/10.1016/j.quageo.2014.12.006, 2015.
Huntley, D. J., GodfreySmith, D. I., and Thewalt, M. L.: Optical dating of sediments, Nature, 313, 105–107, 1985.
Leutz, H., Schulz, G., and Wenninger, H.: The decay of potassium40, Z. Physik, 187, 151–164, https://doi.org/10.1007/BF01387190, 1965.
Mayya, Y. S., Morthekai, P., Murari, M. K., and Singhvi, A. K.: Towards quantifying beta microdosimetric effects in singlegrain quartz dose distribution, Radiat. Meas., 41, 1032–1039, https://doi.org/10.1016/j.radmeas.2006.08.004, 2006.
Megumi, K., Oka, T., Yaskawa, K., and Sakanoue, M.: Contents of natural radioactive nuclides in soil in relation to their surface area, J. Gepphys. Res.Sol. Ea., 87, 10857–10860, 1982.
Mejdahl, V.: Thermoluminescence dating: betadose attenuation in quartz grains, Archaeometry, 21, 61–72, 1979.
Murray, A., Marten, R., Johnston, A., and Martin, P.: Analysis for naturally occuring radionuclides at environmental concentrations by gamma spectrometry, J. Radioanal. Nucl. Ch., 115, 263–288, 1987.
Murray, A. S. and Mohanti, M.: Luminescence dating of the barrier spit at Chilika lake, Orissa, India, Radiat. Prot. Dosim., 119, 442–445, https://doi.org/10.1093/rpd/nci500, 2006.
Murray, A. S. and Wintle, A. G.: Luminescence dating of quartz using an improved singlealiquot regenerativedose protocol, Radiat. Meas., 32, 57–73, 2000.
Murray, A. S., Helsted, L. M., Autzen, M., Jain, M., and Buylaert, J. P.: Measurement of natural radioactivity: Calibration and performance of a highresolution gamma spectrometry facility, Radiat. Meas., 120, 215–220, https://doi.org/10.1016/j.radmeas.2018.04.006, 2018.
Nathan, R. P. and Mauz, B.: On the doserate estimate of carbonaterich sediments for trapped charge dating, Radiat. Meas., 43, 14–25, https://doi.org/10.1016/j.radmeas.2007.12.012, 2008.
Olley, J. M.: The use of ^{232}U and ^{232}Th decay series radionuclides in sediment tracing, Australian National University, PhD thesis, 1994.
Újvári, G., Stevens, T., Molnár, M., Demény, A., Lambert, F., Varga, G., Jull, A. J. T., PállGergely, B., Buylaert, J.P., and Kovács, J.: Coupled European and Greenland last glacial dust activity driven by North Atlantic climate, PNAS, 114, E10632–E10638, https://doi.org/10.1073/pnas.1712651114, 2017.
Zimmerman, D. W.: Thermoluminescent dating using fine grains from pottery, Archaeometry, 13, 29–52, 1971.