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**Solid Earth**
An interactive open-access journal of the European Geosciences Union

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- About
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**Research article**
09 Sep 2019

**Research article** | 09 Sep 2019

Electrical formation factor of clean sand from laboratory measurements and digital rock physics

^{1}Department of Geology, Gombe State University, Gombe, Nigeria^{2}Exploration Geophysics, Curtin University, Perth, Australia^{3}Peter Cook Centre of Carbon Capture and Storage, The University of Melbourne, Melbourne, Australia^{4}CSIRO Energy, Perth, Australia

^{1}Department of Geology, Gombe State University, Gombe, Nigeria^{2}Exploration Geophysics, Curtin University, Perth, Australia^{3}Peter Cook Centre of Carbon Capture and Storage, The University of Melbourne, Melbourne, Australia^{4}CSIRO Energy, Perth, Australia

**Correspondence**: Stephanie Vialle (stephanie.vialle@curtin.edu.au)

**Correspondence**: Stephanie Vialle (stephanie.vialle@curtin.edu.au)

Abstract

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Electrical properties of rocks are important parameters for well-log and
reservoir interpretation. Laboratory measurements of such properties are
time-consuming, difficult, and impossible in some cases. Being able to
compute them from 3-D images of small samples will allow for the generation of a massive amount of
data in a short time, opening new avenues in applied and fundamental
science. To become a reliable method, the accuracy of this technology needs
to be tested. In this study, we developed a comprehensive and robust
workflow with clean sand from two beaches. Electrical conductivities at 1 kHz were first carefully measured in the laboratory. A range of porosities
spanning from a minimum of 0.26–0.33 to a maximum of 0.39–0.44,
depending on the samples, was obtained. Such a range was achieved by compacting the samples
in a way that reproduces the natural packing of sand. Characteristic electrical
formation factor versus porosity relationships were then obtained for each
sand type. 3-D microcomputed tomography images of each sand sample from the
experimental sand pack were acquired at different resolutions. Image
processing was done using a global thresholding method and up to 96
subsamples of sizes from 200^{3} to 700^{3} voxels. After
segmentation, the images were used to compute the effective electrical
conductivity of the sub-cubes using finite-element electrostatic
modelling. For the samples, a good agreement between laboratory measurements
and computation from digital cores was found if a sub-cube size representative elemental volume (REV) was
reached that is between 1300 and 1820 µm^{3}, which,
with an average grain size of 160 µm, is between 8 and 11 grains.
Computed digital rock images of the clean sands have opened a way forward for
obtaining the formation factor within the shortest possible time; laboratory
calculations take 5 to 35 d as in the case of clean
and shaly sands, respectively, whereas digital rock physics computation takes just
3 to 5 h.

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How to cite.

Garba, M. A., Vialle, S., Madadi, M., Gurevich, B., and Lebedev, M.: Electrical formation factor of clean sand from laboratory measurements and digital rock physics, Solid Earth, 10, 1505–1517, https://doi.org/10.5194/se-10-1505-2019, 2019.

1 Introduction

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Electrical formation factor (FF) refers to the ratio of the electrical resistivity of a saturated medium (sediment or rock) to that of the saturating fluid (Guéguen and Palciauskas, 1994). This is an important parameter in exploration geophysics as, contrary to the electrical resistivity of reservoirs that is dependent on the resistivity of the saturating fluid (and hence the same type of reservoir can exhibit high or low resistivities; Constable and Srnka, 2007; Jinguuji et al., 2007; Mitsuhata et al., 2006), the formation factor is an intrinsic property of the rock independent of fluid salinity. Measurement of the formation factor in the laboratory is often difficult and time-consuming, if not impossible in some cases. Minerals forming the rock or sediment sample must reach thermodynamical and electrical equilibrium with the saturating fluid, which typically takes 4 to 6 d in a high-permeability, high-porosity clean sandstone but may require at least 4 to 6 weeks for a tight gas sand or a low-porosity rock or sediment with a high clay content. Furthermore, results are affected by current leakage problems (especially at high frequencies) and electrode polarization (emphasized at low frequencies).

Hence, the computation of electrical properties from microstructural models has been investigated by several teams in the past 50 years. Various methods have been proposed, from statistical models used to reconstruct 3-D porous materials (e.g. Miller, 1969; Joshi, 1974; Milton, 1982; Torquato, 1987; Adler et al., 1990, 1992; Yeong and Torquato, 1998) to direct measurement of a 3-D structure from synchrotron and X-ray computed microtomography (XRCM) (e.g. Dunsmuir et al., 1991; Spanne et al., 1994; Arns et al., 2001; Øren and Bakke, 2002; Nakashima and Nakano, 2011; Øren et al., 2007) or laser confocal microscopy (Fredrich et al., 1995). In most of these studies using XRCM images, the numerical prediction of electrical conductivity underestimates the experimental results by 30 % to 100 % (which leads to an overestimation of the formation factor) (Spanne et al., 1994; Schwartz et al., 1994; Auzerais et al., 1996). Several explanations have been put forward to justify such a discrepancy: percolation differences between the model and real material, mainly due to smaller volume sampling in the model (Adler et al., 1992; Bentz and Martys, 1994); the addition of a third phase to the traditional two-phase model (the rock matrix being one phase and the saturating fluid being a second phase) that counts for the bound fluid at the grain fluid interface (Zhan and Toksoz, 2007); and discretization errors and statistical fluctuations (Arns et al., 2001).

The underlying question behind the computation of electrical properties of digital porous media samples (or any other rock or transport properties) is whether the obtained numerical values are accurate. One aspect of this question relates to the technology itself, namely 3-D imaging, image processing and segmentation, and the suitability and stability of the numerical code. These three key elements of the technology have been investigated by various teams, and the most comprehensive and exhaustive study performed on the various steps of the digital rock physics workflow is the benchmark comparison from Andrä et al. (2013a, b). As they are using various rock types and processing and computing methods, the comparison is complex: they concluded that the computed effective rock properties are affected by segmentation processes, the choice of digital sub-volume, and the choice of numerical code and boundary conditions. Nonetheless, the different values obtained for the formation factor deviated at most by 23 % from the midrange value (Andrä et al., 2013a). For the sphere pack sample, all computed formation factors ranged from 4.3 to 4.8.

The second aspect of this question relates to the comparison of the computed values with laboratory-scale experimental data to validate the correctness of the digital rock physics workflow. However, because both experiments are done at a different scale (centimetre scale for the laboratory and millimetre scale for the digital computation) and because rocks are heterogeneous at all scales, the laboratory-measured and digitally computed values do not have to match. Instead, trends between two properties (e.g. formation factor and porosity) computationally derived and produced in the laboratory should be in good agreement (Dvorkin et al., 2011; Andrä et al., 2013a).

In the work described in this paper, we propose a robust workflow to digitally compute the electrical properties of clean (i.e. that does not contain any clay or other conductive minerals) unconsolidated porous media. We first carefully measure in the laboratory the formation factor of two beach sand samples of similar mineralogy (quartz and carbonate), but of different grain size, over a wide range of porosities obtained by compacting the sand sample. Hence, trends in formation factor versus porosity that reproduce a packing as close as possible to the one found in situ were obtained. We then compute the formation factor from X-ray microtomography images using the free software and finite-element electrostatic code from the National Institute of Standards and Technology (NIST) with multiple subsamples of various sizes. To our knowledge, this is the first time that such work has been done on clean sand.

2 Materials and laboratory methods

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The samples investigated in this paper are sand samples collected from the
coastal margin of the Perth Basin, Western Australia. The Perth Basin is an
elongate, north–south-trending trough underlying approximately 100 000 km^{2} of the Western Australian margin. Sediments were shed from
the adjacent Yilgarn block. The Yarragadee and Leederville sandstone
formations are intercalated with the Tamale limestone that forms the
carbonates at the Upper Cretaceous. One sample was collected from
Scarborough Beach (31^{∘}53^{′}41.97 S, 115^{∘}45^{′}17.74 E) and
one from Cottesloe Beach (31^{∘}59^{′}40.62 S, 115^{∘}45^{′}03.70 E). All the samples are composed of quartz and carbonate in 80 *%* / 20 *%* (volume) proportion, respectively, as determined from the three-phase
watershed segmentation presented in Sect. 3.2.2 of this paper. Grain
size was determined by micro-CT image analysis and is between 16 and 794 µm (median 140 µm) for quartz grains and between 19 and 446 µm
(median 168 µm) for carbonate grains at Scarborough Beach. It is between 17 and 606 µm (median
159 µm) for quartz and between 15 and 415 µm (median 172 µm) for
carbonate grains at Cottesloe Beach. Sand
samples were thoroughly washed clean with tap water to remove any plants and
grass debris. Loose moist sand was then packed into the different cells used
to perform the electrical resistivity measurements, forming an
initially high-porosity loose random pack; decreasing porosity in subsequent
experiments was achieved by shaking the cell and using tied sticks to
compact the sand. This was done in a way to achieve a packing as close as
possible to the one found in situ. A range of six different porosities was obtained
for the Scarborough Beach sand samples, with an initial porosity of 0.40
(loosely packed) down to 0.27 when highly packed, while five and four different
porosities were obtained for the Cottesloe Beach sand, depending on the
geometry of the cell, with the loosely packed sample having a porosity of
0.39 and the highly packed sample having a porosity of 0.30.

Porosity was determined from the weights and densities of the sand grains and the known volumes of cells used in the experiment as

$$\begin{array}{}\text{(1)}& \mathit{\varphi}={\displaystyle \frac{\left({V}_{\mathrm{t}}-m/\mathit{\rho}\right)}{{V}_{\mathrm{t}}}},\end{array}$$

where *ϕ* is porosity, *V*_{t} is the total volume of the cell, *m* is
the average mass of the dry sand before and after the experiment, and *ρ*
is the density of the sand grains. Grain density was measured by He pycnometry
and found to be equal to 2.71 g cm^{−2}.

Two different types of cells are used in the experimental set-ups, which were
utilized to monitor the electrical resistivities of the sand samples as a
function of the salinity of the saturating pore water. The two experimental
set-ups are outlined in Figs. 1 and 2. For the cell called the “flow cell”,
the sample electrical resistances are measured, while saline solutions of
increasing salinities are continuously flooded through the sand samples.
Before proceeding with the next saline solution, the reading of the sample's
electrical resistance is left to stabilize for a few hours. For the cell called
the “static cell”, the sand samples are successively saturated with saline
solutions of increasing salinities, left to equilibrate with no fluid flow until
stability of the sample electrical resistance reading is achieved, and then
drained before saturating the sand sample with the next saline solution.
Thus, the utilization of this cylindrical-shaped static cell drastically
reduces the experimental time; however, the sample preparation for the static
cell is easier than for the flow cell. The flow cell is of cylindrical shape,
27 cm in length, and 5 cm in radius (total volume of 2120.6 cm^{3}), while
the static cell is of rectangular shape, 29.8 cm in length, 8.7 cm in width,
and 6.2 cm in height (total volume of 1607.41 cm^{3}).

Both cells are made up of Perspex (acrylic) and have an outlet and an inlet
connected by tubing to a tank that serves as a reservoir for the various
solutions injected into the sand samples. The solutions flow through the
sand samples via gravity (falling-head method) and, for the flow cell, two
valves at the inlet and outlet are used to achieve a flow rate ranging
from 0.52 to 2.75 mL s^{−1}. This flow rate is continuously recorded.

Injected solutions are fresh and saline solutions made with tap water and
table salt in various amounts: five different salinities of 0, 5, 15,
25, and 35 g L^{−1} were achieved and measured on an electric balance (Napco JA-5000), and
the solution was stirred until complete dissolution of the salt into the water.

Both cells are equipped with two electrodes made of zinc wire gauze with
surface areas of 78.55 and 53.94 cm^{2} for the dynamic and
static cells, respectively. The electrodes are glued at the bottom and at
the lid cover of the cylindrical dynamic cell, while they are fixed on both
sides of the rectangular static cell; the two electrodes of each cell are
connected to an LCR meter (Stanford Research Systems SR720) connected to a laptop to monitor the
electrical resistance of the sand sample. The recording time interval for the
dynamic cell laboratory measurements is taken at 1 min, while the
recording time interval for the static cell laboratory measurement is 10 min. A drive voltage of 1 Vrms is applied and a frequency of 1 kHz is
chosen to minimize the phase angle between the voltage and current (i.e.
electrode polarization). With these conditions, the monitored *Q* factor did not
exceed 0.095, indicating that the system is nearly purely resistive. For the
dynamic cell laboratory measurements, the conductivity of the injected
solutions coming out of the cell is monitored by an encased conductivity
meter (Hanna edge) attached to the cell at intervals of 1 min to make it
synchronous with the sand sample resistance measurements. The fluid
electrical conductivity for the static cell set-up is measured with the same
probe using the saturating solution drained from the sand sample once the
resistance has become stable.

Because the sand samples do not contain any clay and because the injected
solutions have a conductivity (10^{−2} to $\mathrm{5.0}\times {\mathrm{10}}^{+\mathrm{1}}$ S m^{−1}) much larger
than that of quartz or carbonate surface conductivity ($\mathrm{5.4}\times {\mathrm{10}}^{-\mathrm{3}}$ S m^{−1} following
Miller et al., 1988, and $\mathrm{1.4}\times {\mathrm{10}}^{-\mathrm{3}}$ S m^{−1} following Vialle, 2008), surface and matrix electrical conductivities can be neglected
(e.g. Johnson and Sen, 1988; Garrouch and Sharma, 1994). The electrical
formation factor *F* is then given by

$$\begin{array}{}\text{(2)}& F={R}_{\mathrm{s}}{R}_{\mathrm{w}},\end{array}$$

with

$$\begin{array}{}\text{(3)}& {\displaystyle}{R}_{\mathrm{s}}& {\displaystyle}={r}_{\mathrm{s}}{\displaystyle \frac{A}{L}},\text{(4)}& {\displaystyle}{R}_{\mathrm{w}}& {\displaystyle}={\displaystyle \frac{\mathrm{1}}{{\mathit{\sigma}}_{\mathrm{w}}}},\end{array}$$

where
*R*_{s} is the resistivity of the sand sample saturated with water,
*R*_{w} is the resistivity of the water,
*r*_{s} the measured resistance of the sand sample saturated with water, *A* the surface
area of the electrode, *L* the length of the cell, and *σ*_{w} the
measured conductivity of water.

To obtain the formation factor, the sample's resistivity, once it has stabilized, is plotted against the saline water's resistivity, and the formation factor is given by the inverse of the slope. Such a plot is given in Fig. 3 for the example of a Cottesloe Beach sample with porosity 33 %.

3 Digital rock samples and computation of electric properties

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Two samples were prepared for imaging with X-ray microcomputed tomography
(XRMCT): one from Scarborough Beach and one from Cottesloe Beach. Loose sand
was put in a cylindrical Pyrex glass tube of 6 mm diameter and 6 cm
height, and the tube was inserted into the core holder of the microtomograph.
The samples were scanned with the 3-D X-ray microscope Versa XRM 500 (Zeiss–XRadia) using an X-ray energy of 60 keV, a current of 70.66 mA, and a power
of 5 W. In each scan 3000 projections (radiographs) were acquired. The
exposure time was 2 s per radiograph. Initial cone-beam 3-D image
reconstruction was performed using the software XM Reconstruction (XRadia).
A secondary reference was required to remove geometrical artefacts during
reconstruction. After 3-D reconstruction, 3-D volume was sliced onto 2-D images
for further processing. A total of 1021 2-D images for the Scarborough
Beach sample and 991 2-D images for the Cottesloe Beach sample were available for
analysis. Total scanning time was 2 h 55 min and 2 h 42 min for the
Scarborough and Cottesloe samples, respectively. Nominal voxel sizes of
2.5761 and 2.5516 µm^{3} were achieved with
source-to-sample and detector-to-sample distances of 11 and 22 mm, respectively, for the
Scarborough and Cottesloe Beach samples.

We used the software package Avizo Fire 9 (FEI Visualization Sciences Group) for image enhancement and segmentation. Greyscale images of the 2-D slices were processed using a non-local means filter in the intensity range of 255–5344 for Scarborough Beach and 255–5467 for Cottesloe Beach, with the aim of removing ring artefacts in the images and properly enhancing interfaces between the pores and grains as well as removing noise. A non-local means filter has been shown to effectively remove ring artefacts without introducing edge smoothing, in contrast to many other filters, and thus does not require the use of an additional mask (see, for example, the review paper of Schlüter et al., 2014).

Figure 4a–d show raw and filtered images for both Scarborough and Cottesloe Beach: we can easily notice that the quality of the image has increased. In these images, the white grains are carbonate, grey grains are quartz, and black within the disc corresponds to void space (pores).

The filtered images were segmented using two types of thresholding algorithms: the first one resulted in a two-phase segmentation that was further used for computing sample electrical conductivities; the second one was a watershed algorithm that resulted in a two- or three-phase segmentation used for grain analysis. Note that filtering and segmentation workflows were applied to the full 3-D dataset. Figure 5 shows the histogram for both samples.

Because both quartz and carbonate have very low conductivity compared to water, they can be both considered non-conductive for computation purposes of the electrical conductivity of the water-saturated sand sample. Hence, quartz and carbonate can be put in a single phase, and pores will constitute a second phase that will later be filled with a conductive fluid for the computation of sample electrical properties. We use a global threshold segmentation algorithm to separate pores from grains: the set intensity value separating pores from grains (both quartz and carbonate grains having higher intensity values than pores) is kept the same for all 2-D slices.

Poor segmentation can affect the accurate calculation of porosity. To check the
quality of the segmentation, we compare the porosity estimated in the
laboratory with the one estimated from micro-CT scan images. We made a
random loose pack of sand (cm^{3}) in the laboratory to obtain the highest
porosities of 0.361 and 0.349 from Scarborough and Cottesloe beaches,
respectively, while the smaller scanned sample of the sand (mm^{3}) was
also randomly packed in the small tube, from which porosities of 0.369 and
0.359 were obtained from the images of Scarborough and Cottesloe beaches,
respectively.

We used a marker-based watershed segmentation algorithm from Avizo Fire 9. We defined either two or three marker ranges of greyscale intensity: for pores and grains or for pores, carbonate grains, and quartz grains. We then performed a watershed flooding for each of these two or three phases. The two-phase watershed segmentation allows for the computation of pore volume and grain size distribution, whereas the three-phase segmentation (Fig. 6) gives the volume fraction of the different minerals.

From this segmentation, we computed the volume fraction of quartz and carbonate (excluding the pore volume). The result is 81.9 % quartz and 18 % carbonate for the Scarborough sample and 87.8 % quartz and 12.2 % carbonate for the Cottesloe sample.

The 3-D filtered and segmented volumes for each of the two sand samples were
subdivided into overlapping sub-cubes (96 in total) of four different sizes: 3 sub-cubes with a size of 700^{3}, 8 with a size of 500^{3}, 13 with a size
of 350^{3}, and 20 with a size of 200^{3} for the Scarborough Beach
sample, as well as 5 sub-cubes with a size of 700^{3}, 10 with a size of
500^{3}, 13 with a size of 350^{3}, and 24 with a size of
200^{3} for the Cottesloe Beach sample. Porosity was estimated using Avizo
software for each of these 96 sub-cubes.

The 2-D cropped images were then exported in binary format for the computation of electrical properties (Fig. 7).

To estimate conductivity from micro-CT images, we assume that pores are electrically conductive and that the solid phases are not conductive. This assumption is based upon the concept that mainly the ions in fluid-filling pores can be drifted under the effect of external electric fields. To estimate the conductivity from images, we first have to calculate an average current density.

If we assume that the conservation of charge is valid in the pore structure, then no net charges are created or annihilated in the pore volume and pore surfaces; the current density vector obeys the following equation:

$$\begin{array}{}\text{(5)}& \mathrm{\nabla}\cdot J=\mathrm{0}.\end{array}$$

On the other hand, Ohm's law at the microscopic level assumes that the current density is proportional to the electrical potential field:

$$\begin{array}{}\text{(6)}& J={\mathit{\sigma}}_{\mathrm{w}}\mathrm{\nabla}V,\end{array}$$

where *J* is the electrical current density, *σ*_{w} is the electrical
conductivity of the fluid that fills the pore space, and *V* is the electrical
potential field (voltage). By substituting Eq. (6) into Eq. (5), we have
the Laplace equation as

$$\begin{array}{}\text{(7)}& \mathrm{\nabla}\cdot \left({\mathit{\sigma}}_{\mathrm{w}}\mathrm{\nabla}V\right)=\mathrm{0}.\end{array}$$

Equation (7) can be solved numerically for pore structures by applying an
external electric field (*E*_{ext})
on the boundaries. One of most reliable numerical methods to estimate the
average current density from 3-D images is the finite-element method. We use
the same free software written by Garboczi (1998). This method, by
minimizing the electrical energy stored in the porous volume under study,
estimates the local potential fields (*V*) at each coordinate system (pore and
solid phases). For a given microstructure, because of the applied fields or
other boundary conditions, the final voltage distribution is determined by
minimization of the total energy stored in the system (Garboczi, 1998). Figure 8a and b show the potential field variations in Scarborough
and Cottesloe Beach samples, respectively. This can help us evaluate the
effective current density (*J*_{av}) by using Eq. (8) and by taking the volume average of the local
current density vectors (** J**). On the other hand, the volume average of current density is defined as

$$\begin{array}{}\text{(8)}& {\mathit{J}}_{\mathrm{av}}=\langle \mathit{J}\rangle ={\mathit{\sigma}}_{\mathrm{eff}}{\mathit{E}}_{\mathrm{ext}},\end{array}$$

where
*σ*_{eff} is the effective conductivity of the porous medium. Effective conductivity
is a second-rank tensor. In Eq. (7), the current density (*J*_{av}) and the external electrical field (*E*_{ext}) are vectors. If we assume that the external electrical field is
unidirectional (let us assume that in the *x* direction,
$\mathit{E}=E\cdot {\mathit{u}}_{x}$), then the current density can have components on any other directions and
can thus be written in the general form as

$$\begin{array}{}\text{(9)}& {\mathit{J}}_{\mathrm{av}}={J}_{x}\cdot {\mathit{u}}_{x}+{J}_{y}\cdot {\mathit{u}}_{y}+{J}_{z}\cdot {\mathit{u}}_{z}.\end{array}$$

Then, from Eq. (7), the current density can be rewritten as

$$\begin{array}{}\text{(10)}& {\mathit{J}}_{\mathrm{av}}={\mathit{\sigma}}_{xx}E\cdot {\mathit{u}}_{x}+{\mathit{\sigma}}_{yx}E\cdot {\mathit{u}}_{y}+{\mathit{\sigma}}_{zx}E\cdot {\mathit{u}}_{z}.\end{array}$$

In homogenous media, we expect the current density to be negligible in the direction perpendicular to the external electrical fields. This implies that for homogenous media, the effective conductivity tensor is a diagonal matrix. On the other hand, for heterogeneous media, the current density in the direction perpendicular to the external electrical field is not zero or is not small compared to the diagonal values. Hence, in general, the current density is a second-rank tensor of the form

$$\begin{array}{}\text{(11)}& \mathit{\sigma}=\left[\begin{array}{ccc}{\mathit{\sigma}}_{xx}& {\mathit{\sigma}}_{xy}& {\mathit{\sigma}}_{xz}\\ {\mathit{\sigma}}_{yx}& {\mathit{\sigma}}_{yy}& {\mathit{\sigma}}_{yz}\\ {\mathit{\sigma}}_{zx}& {\mathit{\sigma}}_{zy}& {\mathit{\sigma}}_{zz}\end{array}\right].\end{array}$$

The 700^{3} voxel sample from Scarborough was analysed by applying a
current successively in the *x*, *y*, and *z* directions to find out whether the sample
shows some anisotropy (see Fig. 9).

The output of conductivity along the *x*, *y*, and *z* directions shows almost the same
values of the formation factor (5.30, 4.96, and 5.08, respectively). The
difference in the values of formation factor between the *x* direction and
*y* direction is 6.6 %, while that between the *x* direction and *z* direction is
4.4 %; hence, the sample presents a small anisotropy at the scale of
investigation. In the following, we took an average of the conductivities in
the three different directions, which mathematically is equal to one-third
of the trace of the conductivity tensor; for simplicity, we then consider the
conductivity to be a scalar number for all images.

From the effective conductivity calculated for micro-XRCT images, the electrical formation factor can be estimated as

$$\begin{array}{}\text{(12)}& F={\displaystyle \frac{{\mathit{\sigma}}_{\mathrm{w}}}{{\mathit{\sigma}}_{\mathrm{eff}}}},\end{array}$$

where
*σ*_{w} is the electrical conductivity of pore fluids, taken equal to 1 in the
computation. The electrical formation factor is calculated for each of the
different sub-cubes obtained from the micro-CT images of the Scarborough and
Cottesloe Beach samples.

4 Results

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Figure 10 displays the values of the formation factor against porosity for the Scarborough and Cottesloe beaches, computed as described in Sect. 2.2.2 and for each porosity value obtained by compacting the initial sand pack. Correlation coefficients were very good to excellent and varied between 0.975 and 0.999 and between 0.974 and 0.996 for the flow cell for the Scarborough and Cottesloe samples, respectively. They varied between 0.882 and 0.993 and between 0.987 and 0.999 for the static cell for the Scarborough and Cottesloe samples, respectively. The results for both the static and flow cells are reported in Tables 1 and 2 for both samples and for all data points. The values of the formation factors obtained using the flow cell are higher than those obtained using the static cell for both the Scarborough (8.2) and Cottesloe (8.5) Beach samples, whereas for Scarborough Beach, formation factors have close values at high porosities and then depart from each other at lower porosities (lower than 0.39). Some deviations between the results obtained for both static and flow cells may be due to non-uniform compaction of the samples in the case of the flow cell and/or non-complete fluid replacement in the case of the flow cell. In these figures, we have bounded the experimental data by two lines that represent a power-law relationship between the formation factor and porosity in the form

$$\begin{array}{}\text{(13)}& F=a\cdot {\mathit{\varphi}}^{-m}={\mathit{\varphi}}^{-m}.\end{array}$$

This is Archie's law (Archie, 1942) with a tortuosity factor *a* of 1.
The tortuosity factor usually ranges from 0.5 to 1.5, but there has been
quite a wide range reported in the literature for sand, from the most used value
of 0.62 (Humble formula; Winsauer et al., 1952) to up to 2.45 (Porter and Carothers, 1970). We take the same tortuosity factor value of 1 for all
samples. This is the value for clean granular formations (Sethi, 1979).

Formation factors were plotted against porosity for all the micro-CT scan image cubes for Scarborough and Cottesloe beaches (Fig. 11).

Similarly, both porosity and formation factor were plotted against the cube
sizes 200^{3}, 350^{3}, 500^{3}, and 700^{3} (Figs. 12 and 13, respectively). Scattering is shown
when the cube sizes were small, which begins to level off as the
representative elemental volume (REV) is approached. This REV is somewhere
between 500^{3} and 700^{3}, which corresponds to a sample size
between 1.3 and 1.8 mm^{3}.

5 Discussion

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As noted earlier in Sect. 4.1, the values of the formation factor obtained
by the static cell are higher than those obtained by the dynamic cell (for a
given porosity) for both samples. This translates into a higher cementation
exponent *m*. One reason for this can be the design of the cell itself and
the way to achieve a stable reading of sample conductivity for each fluid
salinity. In the rectangular (static) cell, because the higher-salinity
brine is introduced or retrieved via the centre of the panels (see Fig. 2),
there could some brine left in the corners that will only equilibrate with
the new injected brine by diffusion, and hence there could be a lower
conductivity of the brine in these corners compared to the conductivity of
the injected brine. As a result the measured sample conductivity will be
lowered with respect to what it should be, giving a higher ratio of sample to
brine conductivities (i.e. formation factor; see Eq. 11). Using a
cylindrical cell thus has the advantage of providing a better replacement of
the brine.

Figure 14 shows reported data from both the literature and those acquired in
this study for the Cottesloe and Scarborough Beach samples (using the flow
cell). Data from the literature include natural sand samples and synthetic
granular media made of plastic particles with a regular geometrical shape
(Wyllie and Gregory, 1953). We have bounded these data by the relationship
presented in Eq. (14), with *m*=1.3, which corresponds to the original work of
Archie (1942) for unconsolidated media, and by the same relationship, with
*m*=1.8, for the upper bound. We see in this figure that our experimental
results for the Cottesloe and Scarborough Beach samples are in agreement with
data reported for other beach sands. Considering the data reported in this
figure, we observe that Archie's classical formula for unconsolidated media
underestimates the formation factor and that the departure from sphericity
leads to a larger *m* coefficient. Since Archie's work, many authors have
proposed alternative formation factor–porosity relationships. Winsauer et
al. (1952) suggested that *a*≠1 in Eq. (14) is a better expression, whereas
other authors derived a non-power-law dependency on porosity. From a
practical point of view, no formula relating the formation factor to
porosity for unconsolidated media fits all the experimental data, and, for a
given porosity, the formation factor depends on the particle geometry,
particle size distribution, and subsequent packing.

In Fig. 15, we compare laboratory data to computed data. Laboratory data
are those acquired with the flow cell, which, as discussed earlier in this
section, is expected to give more reliable data. Computed data are those
obtained for a cube size of 700^{3}, which is above the REV, as
presented in Sect. 4.2. We can see that there is an excellent agreement
for the Cottesloe Beach sample and a good agreement for the Scarborough Beach
sample. At this stage, it is difficult to explain why one sample gave better
agreement and whether it is an experimental error or the
higher content of carbonate grains for the Scarborough sample that makes the
computation less accurate: indeed, carbonate grains may present some
intra-porosity (for example, micritic phases) and thus have an electrical
conductivity.

6 Conclusions

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The electrical properties of rocks are important parameters for well-log and reservoir interpretation. Laboratory measurements of such properties are time-consuming, difficult, and even impossible in some cases. In view of this, we have successfully combined the scientific approach of laboratory measurements (as a benchmark) with micro-CT scan computational images. We have thereby achieved the objective of determining the variability of computed formation factors as a function of porosity from laboratory measurements and micro-CT scan images from two sand samples for Scarborough and Cottesloe beaches in Perth Basin. This is the fastest method of obtaining a formation factor from CT scan images, which takes less time (5–7 h), while calculations from laboratory measurements take much more time (5 to 30 d or more).

This approach is practical, easily repeatable in real time (though
expensive), and can be an alternative method for calculating a formation factor
when time is not on the side of the experimenter, which is always the case.
Results of images below 500^{3} (Scarborough) and 350^{3} (Cottesloe)
indicate that they are not suitable REVs for pore-scale networks.

In this paper, a micro-CT scan image computational technique was employed to calculate properties such as porosity and formation factor on large three-dimensional digitized images of a sand sample. We demonstrated that for most of the parameters studied here, the values obtained by computing micro-CT scan images agreed with classical laboratory measurements and results from other researchers. This work was focused on establishing a robust methodology and workflow, and we thus started with one of the most simple materials, though it is still highly relevant for many applications in oil and gas or water management environments. For more complex geological materials, such as low-permeability rocks, multi-mineralitic rocks, and materials with conductive minerals, further developments are obviously needed. However, these developments are mostly related to the employed techniques (e.g. a higher-resolution imaging technique would be needed for low-permeability rocks, a more complex laboratory set-up, and techniques for measurements of rocks with conductive minerals or minerals with a non-negligible surface conductivity, etc.) rather than to the overall workflow established here (comparison between laboratory and computed data through trends between properties).

Data availability

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Data availability.

All data shown in Figs. 10 to 15 (except those taken from previous studies by other authors in Fig. 15 that are displayed for comparison) are given in Tables 1 and 2. X-ray images are available on request from the authors.

Author contributions

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Author contributions.

MAG carried out the experiments and performed the numerical simulations; SV and ML designed and planned the experiments; MM supervised and verified the numerical simulations; MAG wrote the paper in consultation with SV, MM, ML, and BG. BG initiated the project. SV conceived the original idea and supervised the project.

Competing interests

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Competing interests.

The authors declare that they have no conflict of interest.

Acknowledgements

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Acknowledgements.

We thank Dominic Howman and Vassili Mikhaltsevitch for help in cell design and laboratory experiments and Andrew Squelch for help with image processing.

Review statement

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Review statement.

This paper was edited by Ulrike Werban and reviewed by five anonymous referees.

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