A. Diffraction experiment

Shale is a sedimentary rock and composed of a wide variety of minerals. Sheet silicates comprise a large volume fraction of shales and align preferentially parallel to the bedding plane during sedimentation and compaction. Crystallographic preferred orientation (CPO) of phyllosilicates is of great interest, because it is the primary cause of elastic anisotropy observed during seismic prospecting of oil and gas deposits. Thus several studies have focused on improving synchrotron X-ray techniques to quantify textures and microstructures of shales (e.g., Wenk et al., Reference Wenk, Voltolini, Kern, Popp and Mazurek2008; Lutterotti et al., Reference Lutterotti, Voltolini, Wenk, Bandyopadhyay and Vanorio2010; Kanitpanyacharoen et al., Reference Kanitpanyacharoen, Wenk, Kets, Lehr and Wirth2011, Reference Kanitpanyacharoen, Kets, Wenk and Wirth2012a; Vasin et al., Reference Vasin, Wenk, Kanitpanyacharoen, Matthies and Wirth2013).

For this tutorial we use a sample of Kimmeridge shale from the North Sea, UK (Hornby, Reference Hornby1998; Vasin et al., Reference Vasin, Wenk, Kanitpanyacharoen, Matthies and Wirth2013). The sample is a slab, 2 mm thick [Figure 1(a)]. It was measured at the APS high-energy beamline ID-11-C during the same session as the nickel coin discussed in the companion paper (Lutterotti et al., Reference Lutterotti, Vasin and Wenk2014). The wavelength was 0.107 98 Å, and the beam size 0.5 × 0.5 mm. Therefore, the same instrument parameters could be applied which were obtained by refining the CeO₂ standard (see Part I.III). However, samples can shift, so here we will use a slightly different approach as described in detail in Appendix I. This will illustrate the flexibility of MAUD in assigning sample and image orientations relative to the MAUD coordinate system [Figure 1(b)]. During X-ray exposure the sample was translated along the horizontal axis from −2.5 to +2.5 mm to increase the probed volume, and rotated around the horizontal axis (Figure 1 in Lutterotti et al., Reference Lutterotti, Vasin and Wenk2014), from −45° to +45° in 15° increments (i.e., there are seven diffraction images) to obtain adequate pole figure coverage. For the coin we used Y _M as the rotation axis, here we will use Z _M [Figure 1(b)]. The reason for the change in coordinate systems is that this way the pole to the bedding plane of the shale is located in the center of the pole figure and axial symmetry can be imposed. Since the texture describes the preferred orientation of crystals relative to sample coordinates, care must be taken that this relationship is not lost during rotations.

Figure 1.

(a) Slab of shale embedded in epoxy and mounted on a pin. (b) Pole figure coverage with a single image, bedding plane normal is in the center of the pole figure. When fiber symmetry is imposed, each point covers a circle. (c) Coverage with seven images recorded at different sample rotations φ around the Z _M axis.

Images were collected with a Perkin Elmer amorphous silicon detector with dimensions of 2048 × 2048 pixels and a pixel size of 200 × 200 µm. The detector was approximately 1850 mm from the sample. Figure 2(a) shows a diffraction image with many Debye-rings from at least six major phases at different 2θ angles. Several rings display strong intensity variations due to preferred orientation.

Figure 2.

2D synchrotron diffraction images. (a) Kimmeridge shale with many phases, some with strong preferred orientation. (b) LaB₆ standard used for the DAC experiment, rather coarse-grained and with some impurities. (c) Radial diffraction DAC experiment on ferropericlase. Arrow points to a diffraction spot from diamond. The compression direction is vertical.

B. Preliminary analysis for axial symmetry using one image

Refining seven images simultaneously with a number of low-symmetry phases is time-consuming [two-dimensional (2D) diffraction images are integrated in angular azimuthal increments, resulting in a total of several hundred patterns]. Thus it is more efficient to start with only one image measured at φ = 0° [coverage in Figure 1(b)]. Later, we will add the other images in different datasets to complete the analysis [coverage in Figure 1(c)]. The procedure with a single image is justified, because shale textures have approximately axial (fiber) symmetry about the bedding plane normal (transverse isotropy). By imposing this sample symmetry, complete pole figure coverage is obtained with only one dataset. If the texture is not too strong, one can initially assume a random orientation to simplify the first refinement steps and introduce the texture later with the additional images. In case of a very strong texture, we have to work from the start with all images and a complete texture model, but this is not the case for the shale example.

We start from an instrument calibrated with the CeO₂ standard and use the same procedure as for the coin analysis (Part I.IV) to load and integrate the first image. Compared to the coin, we do not rotate the image 90° counterclockwise in ImageJ before processing, so that the horizontal axis is in the center (Z _M) for the shale sample; in this way the bedding plane normal is in the center of the pole figure [see Figures 1(b) and 1(c)]. Since the texture of shale is smoother than the coin [see Figure 2(a)] we can employ a larger integration step of 10°; this reduces the total amount of data to analyze without loss of information and with an increase in speed of the computation. Initially we restrict the refinement range to 2θ = 0.3–3.0° since shale contains several low-symmetry phases with many diffraction peaks that overlap at higher 2θ. Those peaks do not provide much information for texture analysis. Restricting the range greatly speeds up the computation. If necessary, the range can be enlarged at the end of the refinement.

Figure 3 (bottom) displays the stack of experimental diffraction patterns taken at each 10° increment in eta (η). The pole figure coverage is shown in Figure 1(b) with the pole to the bedding plane at Z _M (φ rotation axis).

Figure 3.

Stack of diffraction patterns for Kimmeridge shale, φ = 0° tilt image. Experimental data at bottom and Rietveld fit on top. Some diffraction for lines for illite-smectite (IS), illite-mica (IM), kaolinite (K), quartz (Q) and pyrite (P) are labeled.

We use a fourth-order polynomial background common to all patterns (5 coefficients). However, we must also correct for small angle scattering from platelet-shaped phyllosilicate nanoparticles, which is most visible in the diffraction image at very low angles (2θ ≈ 0.1–0.2°), near the beamstop [Figure 2(a)]. Since these platelets are oriented, small angle scattering displays azimuthal intensity variations. The broad low-angle peak extends as elevated background to the first diffraction peaks of phyllosilicates (2θ ≈ 0.3–0.6°) (Figure 3). To fit this peak, we use two symmetrical background peaks, which are pseudo-Voigt functions that can be positioned arbitrarily in a dataset at any coordinates. The principal one is 2θ [parameters are intensity, 2θ position, half-width at half-maximum (HWHM) in 2θ, and the Gaussian content], but it may span over η (adding a position, HWHM and Gaussian content in η) as well as position angles (χ, φ). Background peaks are useful to model some well-defined bumps occurring in images that do not belong to diffraction from a phase. For details, see the tutorial in Appendix 1.

We limit the refinement to the five major phases: quartz, pyrite, kaolinite, illite-mica, and illite-smectite. There are minor phases such as feldspars with <5% volume and no significant texture. Quartz and pyrite structures can be found in the Crystallography Open Database (Gražulis et al., Reference Gražulis, Chateigner, Downs, Yokochi, Quirós, Lutterotti, Manakova, Butkus, Moeck and Le Bail2009) or in the small database included with MAUD (structures.mdb). We added the following structures to this tutorial: triclinic kaolinite (Bish and Von Dreele, Reference Bish and Von Dreele1989), monoclinic illite-mica (Gualtieri, Reference Gualtieri2000), and monoclinic illite-smectite (Plançon et al., Reference Plançon, Tsipurski and Drits1985). The corresponding Crystallographic Information Files (.cif) are available in the on-line material supplied with the tutorial. For monoclinic phases, the first monoclinic setting has to be used to work with texture (Matthies and Wenk, Reference Matthies and Wenk2009). All texture models implemented in MAUD have been written for the monoclinic “c-unique” setting (i.e., α = β = 90° and γ ≠ 90°); otherwise crystal symmetries are not imposed correctly in orientation space. In MAUD one can change from one setting to another simply by editing the phase and under the “General” tab, selecting the desired setting in the “Space Group” drop-down list. Lattice parameters and atomic positions are adjusted automatically, for example, for the illite-mica phase changing from MAUD settings of C2/c:b1 to C2/c:c1, which selects c for the unique (twofold) axis. Note that the “1” at the end of the space group symbol stands for the first origin and the setting letter is after the colon. The provided .cif file for illite-smectite is already in the first (c-unique) setting.

When multiple phases are entered, MAUD automatically assigns to each added new phase the volume fraction equal to 1/(the total number of phases in the sample). In Rietveld programs, each phase has an assigned scale factor, and each scale factor is optimized during the refinement. Then, from the refined scale factors, the volume and weight fractions of the phases are computed. In addition to volume fraction, the scale factor contains information about the beam intensity and other factors such as absorption, yet it is treated as a unique parameter. If the phases are textured we need an approach that models the sample correctly and uses phase fractions, beam intensities, and absorption corrections (Lutterotti et al., Reference Lutterotti, Voltolini, Wenk, Bandyopadhyay and Vanorio2010), which all contribute to peak intensities and thus may complicate intensity. In our final model, fitting to data from all seven images, we will have a beam intensity parameter for each image, but all patterns in each image have the same beam intensity. Furthermore, we refine the phase fractions for all phases minus one. MAUD imposes that the sum of all phase fractions should be equal to 1 and enforces the volume fraction of the unrefined phase to be the complement to 1.

With a complex sample such as this shale, it is important to provide reasonable initial estimates of phase volume fractions. This avoids divergence of the solution in the initial steps of the least-squares algorithm. Weight fractions are calculated automatically by MAUD, using the provided atomic structure and unit-cell parameters.

For texture, with the initial simplified model using only one image, we need to impose the axial symmetry that MAUD always imposes around the center of the pole figure [Figures 1(b) and 1(c); for the MAUD angle convention and transformations, see also Grässlin et al., Reference Grässlin, McCusker, Baerlocher, Gozzo, Schmitt and Lutterotti2013 and Figure 4(a) in Part I].

Figure 4.

Two diffraction patterns of Kimmeridge shale with scattering lattice planes parallel to bedding plane on top and perpendicular to it at bottom. Crosses are measured data and line is Rietveld fit. Below the patterns is a list of contributing phases and their corresponding diffraction peak positions are marked with ticks. Some diffraction peaks are labeled (IS, illite/smectite; IM, illite/muscovite; Q, quartz; P, pyrite).

After manually adjusting some parameters, such as unit-cell parameters, beam intensity, and background to better fit the experimental patterns (in the parameter list in the MAUD main window, adjust numbers in column “Value”), we start by refining some basic parameters. In the Rietveld refinement procedure, it is always better to avoid refining too many parameters at the beginning and to “guide” the program to the solution. There are normally three major steps to follow: (1) refine background parameters and intensities (scale factors or in MAUD beam intensities and phase fractions); (2) refinement of parameters connected to the peak positions (unit-cell parameters and 2θ errors); and (3) refine microstructural parameters such as crystallite sizes and microstrain. While doing subsequent refinements, one should not change the setting for the refinement of previously refined parameters; the goal is to slowly add additional parameters to the fit. When do we refine texture-related parameters? If the texture is smooth, or weak, it is done at the end (a fourth step), to avoid refining texture instead of some other parameter that could impose intensity variations (e.g., absorption). However, if the texture is sufficiently strong we introduce the texture refinement along with the refinement of intensities in the first step, as long as diffraction peak positions are well constrained. The crystal structure details (e.g., atomic positions and even lattice parameters) should be refined only if necessary and only for phases with sufficient volume fractions and visible peaks. Also, one should use only a single overall atomic displacement parameter (B factor, which is sometimes called temperature factor) by clicking on “Bound B factor” button in the parameter list. When working at high-energy X-rays and very low 2θ angles (available 2θ range is restricted) the data are practically insensitive to B factors. As in the case of the coin in Part I, we should refine the x and y image centering errors as we cannot assure that the CeO₂ calibrant was in the center of the beam, whereas for the shale the beam is inside the sample.

Looking at Figure 3, diffraction peaks of kaolinite (K), illite-mica (IM), and illite-smectite (IS) show strong η-dependent intensity variations indicative of texture. The intensities of the quartz (Q) and pyrite (P) diffraction peaks are almost constant, except for several increased intensity spots because of scattering from larger grains (e.g., P 111 peak). Thus, we only refined preferred orientations of the three phyllosilicates but not of quartz and pyrite. We used the E-WIMV model (Part I.IV) for the kaolinite and the illite-mica with a rather large cell size of 10° in orientation, space given the smooth character of the texture. In general, one should not select a smaller cell size than the measured grid in patterns (in this case it is defined mostly by 10° integration sectors).

For illite-smectite with a well-defined orientation, we use the so-called standard functions method to introduce this capability (Matthies et al., Reference Matthies, Vinel and Helming1987 and implemented in MAUD by Lutterotti et al., Reference Lutterotti, Bortolotti, Ischia, Lonardelli and Wenk2007). The advantage of this approach is that we can describe preferred orientation with some well-defined functions with only few parameters. MAUD implements Gaussian or Lorentzian fiber components (having a fiber symmetry character) and spherical components (also Gaussian, Lorentzian, or mixed). For both types of components, we refine their position in the orientation space, width (in degrees), and Gaussian or Lorentzian character (a single mixing parameter). For the position, the fiber component is defined by the fiber axis orientation with respect to the sample normal (azimuthal PhiY and polar angle ThetaY) and the orientation axis in the unit cell (also two angles: the azimuthal angle around the c-axis PhiH and the polar angle starting from the c-axis ThetaH; see for analogy the angles Φ and β in the appendix of Popa, Reference Popa1992). Standard function texture corrections are very quick to compute and converge rapidly. Another advantage of the standard functions is that they can model very smooth or very strong textures up to epitaxial films, or even single-crystal-like patterns, depending on the width of the component. We defined the fiber axis here parallel to the bedding plane normal [corresponding azimuthal and polar angles are equal to zero, Figure 1(c)]. For the crystallographic texture orientation, we know that the h00 maximum is in the center of the pole figure (monoclinic first setting) and we set the azimuth PhiH to 90° and the polar angle ThetaH to 0°. In this case, we do not refine the orientation angles, as they do not deviate from the imposed starting values, and only the width and Gaussian/Lorentzian mixing parameter of the fiber component will be refined.

The illite-smectite peaks are unusually broad and asymmetric (Figure 4) because of turbostratic disorder, which is typical of clay minerals. This kind of disorder can be described with the Ufer single-layer model (Ufer et al., Reference Ufer, Roth, Kleeberg, Stanjek, Dohrmann and Bergmann2004). The model is very effective in reproducing the asymmetric broadening caused by the turbostratic disorder and can be coupled with the texture analysis (Lutterotti et al., Reference Lutterotti, Voltolini, Wenk, Bandyopadhyay and Vanorio2010). We only need to define the faulting direction (h00) for the smectite and the supercell dimension to approximate the disordered structure. We choose ten times the a-axis (first monoclinic setting) as a sufficient value to model the disorder.

In Figure 3 (top), we can see the resulting 2D plot after the initial refinement with one image and the agreement with the experiment is very good (Figure 3, bottom). Figure 4 shows two individual patterns, one with scattering vectors parallel to, and the other perpendicular to the bedding plane normal and also good agreement for both is observed here. The tickmarks at the bottom denote peaks belonging to each phase. This is the quality that fit users should aim for. Table I lists refined volume and weight fractions for the phases and Table II gives information about the texture. Corresponding pole figures are shown in Figure 5(a) in equal-area projection. Note that illite-mica has the strongest texture and illite-smectite shows the broadest OD. The R-factors, which measure the overall goodness of fit between the model and experimental data, were: R _w = 12.5% and R _b = 8.9% for the single image refinement. In general, R-factors smaller than 15% typically demonstrate a very good refinement.

Figure 5.

Pole figures of basal planes of kaolinite, illite-mica and illite-smectite for Kimmeridge shale after exporting the ODs from MAUD and processing them with BEARTEX. (a) Derived from a single image, imposing fiber symmetry. (b) Result for seven images without imposing symmetry. The corresponding pole figure coverage is shown in Figure 1(c). Equal area projection on the bedding plane, contours in multiples of a random distribution.

Table I.

Phase volume and weight fractions of minerals in shale (in %), with and without imposed axial symmetry of texture, and also using full 2θ range.

Table II.

Texture information for phyllosilicates in shale after processing in BEARTEX, pole densities in m.r.d., with and without imposed axial symmetry of texture, and also using full 2θ range.

C. Analysis without imposing texture symmetry

With this preliminary refinement, we can add the other six diffraction images and proceed with the full analysis. In the end we can also enlarge the refinement range.

With all the seven images rotated in 15° φ increments around Z _M and integrated in 10° sectors around η, the pole figure coverage is now as shown in Figure 1(c). With the larger OD coverage we can analyze the full texture without imposing sample symmetry and use E-WIMV, also for the illite-smectite. In E-WIMV, the default in MAUD is to use all the reflections in the computing range. Contrary to the classical WIMV and pole figure texture analysis, in Rietveld/E-WIMV the pole figure value is weighted using the square root of the theoretical integral intensity of the reflection [Eq. (2) in Lutterotti et al., Reference Lutterotti, Chateigner, Ferrari and Ricote2004]. In this case, if we use the full range, the three textured phases have many overlapped and very weak reflections, even up to 3° in 2θ. Weak overlapped reflections do not contribute significantly to the OD and introduce noise. The texture analysis improves if such reflections are not used, as long as there is no problem with coverage. E-WIMV and WIMV have an option to reject reflections with either small intensities relative to the strongest reflection or d-spacings lower than a threshold value. In the present analysis, we use these options and avoid reflections with intensity <2% of the strongest reflection and with d-spacings smaller than 1.5 Å.

Figure 6 shows the final fit to all seven diffraction images with a cumulative plot of all patterns for the dataset φ = 0° and a 2θ range 0.4–7.8°. At low angles kaolinite, illite-mica and illite-smectite peaks dominate the pattern, whereas at high angles quartz and pyrite dominate. In a case like this, it is important to check the B factors. Wrong B factors for the pyrite/quartz and the other low angle phases may lead to angular-dependent errors that will greatly affect the phase fractions between the “low angle” and “high angle” phases.

Figure 6.

Cumulative plot for all patterns of the φ = 0 image at the end of refinement cycles with seven images, full 2θ range. Dots are experimental data and line is Rietveld fit. Some diffraction peaks are labeled (IS, illite/smectite; IM, illite/muscovite; Q, quartz; P, pyrite).

Pole figures of phyllosilicates, corresponding to those in Figure 5(a), but without imposing symmetry, are shown in Figure 5(b). Note that these pole figures look slightly different from what the reader might see in MAUD. This is because the OD data have been exported from MAUD and were replotted in the software BEARTEX (Wenk et al., Reference Wenk, Matthies, Donovan and Chateigner1998), in order to alleviate artifacts from the cell structure by smoothing and plotting all pole figures on the same scale. In Figure 7, we also show pole figures (100) of kaolinite and (010) of illite-mica and illite-smectite that display a peripheral circle.

Figure 7.

Pole figures 100 of kaolinite and 010 of illite-mica and illite-smectite for Kimmeridge shale without imposing sample symmetry. The corresponding pole figure coverage is shown in Figure 1(c). Equal area projection on the bedding plane, contours in multiples of a random distribution.

In this tutorial presentation, we have started with a single image and imposed axial symmetry, then progressed to many images with no symmetry. This was done to progress from a simple to a more complex analysis. In reality one may want to progress the opposite way: first, with many images, verifying sample symmetry; second, performing necessary sample rotations to bring sample symmetry axes to coincidence with MAUD coordinates, and finally imposing symmetry with one image (for axial symmetry) or several images for more complex sample symmetries.

Pole figure coverage is an important issue, particularly for phases with low crystal symmetry. Shales have very special textures with a maximum pole density corresponding to sheet silicate platelets lying in the bedding plane (Figure 5). This maximum has been well sampled with the present coverage [Figure 1(c)]. However, directions in the bedding plane and particularly in the X _M direction have minimal coverage (Figure 7). The pole figures in Figure 5(b) show minor deviations from axial symmetry, particularly an elongation of the pole figure maxima in the vertical direction for (001) in kaolinite and (100) in illite-mica and illite-smectite. This distortion extends into the blind region of coverage [Figure 1(c)] and may be an artifact. This is further supported by the fact that the maximum pole densities are higher if the axial symmetry is imposed (Table II). Only additional measurements with rotations around other sample axes and combining the data could refine the preferred orientation pattern, but this goes beyond the purpose of this tutorial. One may also want to use a different sample geometry, such as a cylinder instead of a slab, and rotate it from φ = −90° to φ = +90°, collecting 13 images.

Phase volume fractions for Kimmeridge shale without imposing sample symmetry are compared in Table I with results for axial symmetry. They are very similar. For the Kimmeridge shale, the final Rietveld R _w factor is 10.9% (R _b = 8.2%) for the refinement in the 2θ range up to 3°. A few peaks are missing from the calculated diffraction pattern, some are too intense, and some have wrong shapes (e.g., Figures 3 and 4). The missing peaks are mostly because of a feldspar phase that could be entered into the refinement, but we opt to not do so. Anisotropic crystallite shapes and microstrains could also be imposed for phyllosilicates. We have used a CeO₂ powder to refine instrumental parameters (Part I), but CeO₂ has no diffraction peaks at 2θ < 2°. Thus the function describing the instrumental part of diffraction peak broadening (especially the asymmetry) is poorly constrained for this shale with diffraction peaks down to 2θ ≈ 0.5°. Parts of the instrumental peak shape function (the asymmetry) can be refined, as has been done for the full range analysis (see Figure 6). The final R _w for the refinement of the full range and all seven images was reduced from the one image refinement to 10.3% (R _b = 7.4%), which is a very good value, given the number of patterns and complexity of the phases.

A. Experiment

Rietveld texture analysis of synchrotron diffraction images can be applied to study in situ deformation at high pressures with a DAC in radial diffraction geometry (rDAC) (e.g., Merkel et al., Reference Merkel, Wenk, Shu, Shen, Gillet, Mao and Hemley2002; Wenk et al., Reference Wenk, Lonardelli, Merkel, Miyagi, Pehl, Speziale and Tommaseo2006). This proves to be an important method to determine deformation mechanisms at ultrahigh pressures, as in the deep Earth (e.g., Miyagi et al., Reference Miyagi, Kanitpanyacharoen, Kaercher, Lee and Wenk2010) to explain observed seismic anisotropy in the lower mantle and inner core, and to study crystal orientation changes during phase transformations (e.g., Miyagi et al., Reference Miyagi, Kunz, Knight, Nasiatka, Voltolini and Wenk2008; Kaercher et al., Reference Kaercher, Speziale, Miyagi, Kanitpanyacharoen and Wenk2012; Kanitpanyacharoen et al., Reference Kanitpanyacharoen, Merkel, Miyagi, Kaercher, Tomé, Wang and Wenk2012b). The method can also be applied to analyze data from multi-anvil experiments such as D-DIA (e.g., Wenk et al., Reference Wenk, Ischia, Nishiyama, Wang and Uchida2005, Reference Wenk, Kaercher, Kanitpanyacharoen, Zepeda-Alarcon and Wang2013).

The geometry of a typical rDAC deformation experiment is shown in Figures 8(a) and 8(b). Diamonds not only impose pressure, but also deviatoric stress that deforms crystals in the aggregate. The diamond cell is set up in radial rather than axial geometry, i.e. the X-ray beam passes through the sample perpendicular to the compression direction [Figure 8(b)] so that the diffraction image records reflections from lattice planes oriented from parallel to perpendicular to compression [Figure 2(c)]. Preferred orientation is expressed in the azimuthal intensity variations, similar to the images of the shale [Figure 2(a)]. Many DAC experiments, not concerned with stress and texture, use axial geometry, where the X-ray passes through the diamonds and parallel to the compression direction.

Figure 8.

(a, b) Schematic sketch illustrating the geometry of deformation experiments in a DAC in radial diffraction geometry. (c) Actual diamond culets compressing a sample contained by a gasket. (d) Pole figure coverage for the ferropericlase DAC experiment (equal area projection, upper hemisphere). A gap is visible where one pattern is disabled because of the beam stop blocking diffracted X-rays. Direction of incident X-ray beam is shown by arrow. (e) Experimental pole figure data for three reflections.

rDAC experiments have been performed at room temperature to pressures as high as 200 GPa on iron (Wenk et al., Reference Wenk, Matthies, Hemley, Mao and Shu2000) and 185 GPa on MgSiO₃ post-perovskite (Miyagi et al., Reference Miyagi, Kanitpanyacharoen, Kaercher, Lee and Wenk2010). More recently texture measurements have been made in the rDAC on ferropericlase (Mg,Fe)O at 2273 K and ≈ 65 GPa, using a combination of resistive and laser heating (Miyagi et al., Reference Miyagi, Kanitpanyacharoen, Raju, Kaercher, Knight, McDowell, Wenk, Williams and Zepeda2013).

Contrary to the coin and shale experiments, we must take into account changes with pressure, and particularly the macroscopic stress field, which imposes anisotropic elastic distortions of the lattice. As an example we use ferropericlase (magnesiowuestite), which has been previously investigated with rDAC experiments (e.g., Merkel et al., Reference Merkel, Wenk, Shu, Shen, Gillet, Mao and Hemley2002; Kunz et al., Reference Kunz, Caldwell, Miyagi and Wenk2007; Lin et al., Reference Lin, Wenk, Voltolini, Speziale, Shu and Duffy2009; Kaercher et al., Reference Kaercher, Speziale, Miyagi, Kanitpanyacharoen and Wenk2012). This particular sample (Mg_0.75Fe_0.25)O has been described by Kunz et al. (Reference Kunz, Caldwell, Miyagi and Wenk2007).

The rDAC experiment was performed at the high-pressure beamline 12.2.2. of the Advanced Light Source at Lawrence Berkeley National Laboratory. Ferropericlase powder was loaded into a boron-kapton gasket. The initial sample diameter was 80 µm with a starting thickness of 50 µm. The sample was compressed in an rDAC, using diamond anvils with 300 µm diameter culets [Figure 8(c)]. Diffraction images were recorded with a Mar345 image plate detector, with dimensions of 3450 × 3450 and a pixel size of 100 × 100 µm, positioned approximately 285 mm from the sample with an X-ray wavelength of 0.495 94 Å.

There are two immediate complications. First, the beam passes not just through the sample, but also through a gasket, which is needed to maintain pressure. Thus there are additional diffraction lines from the gasket material, especially at low angles [Figure 2(c)]. Gaskets for radial DAC experiments must be made of materials that scatter as little as possible. At lower pressures, amorphous boron (<100 GPa) has been used, while at higher pressure, cubic boron nitride or beryllium have been used. For beryllium, which scatters more, it is advantageous to tilt the cell to have minimum beam interference. If the cell is tilted significantly, the tilt needs to be accounted for by entering the appropriate sample rotation angles in MAUD. Bright diffraction spots from the diamond may also appear in the diffraction pattern. In fact, the large spot on the left side of Figure 2(c) (arrow) is because of diamond. This effect can be minimized by slightly rotating or tilting the DAC. Intense spots can also be masked in image processing.

A second complication is imposed anisotropic elastic strain. Lattice plane spacings are smaller in the compression direction and larger perpendicular to the compression axis. Thus, the Debye rings appear not as circles but as ellipses. The resulting sinusoidal variations of the diffraction peak positions with azimuthal angle are best seen with remapped coordinates, as unrolled images [Figure 9(a), bottom].

Figure 9.

Measured (bottom) and calculated (top) diffraction patterns for ferropericlase; (a) at the beginning of the refinement. Lattice parameters are wrong and there is no texture or anisotropic stress in the model. Also note the black diffraction spot from diamond at 2θ = 23.5°. (b) At the end of the refinement there is an excellent match in position, width and intensity. The compression direction σ is indicated by the black arrow in (a) (larger 2θ angle corresponding to smaller d-spacing).

Ideally the rDAC data analysis should be performed immediately during the DAC experiment, at least through the basic steps. This is necessary, for example to refine lattice parameters and be able to estimate pressure from the equation of state. Thus parameter files with general information should be set up in advance.

B. Initial setup

C. Stress models

D. Refinement

In this case, the refinement is quite complex involving strong texture and high stresses with limited data. We need to guide the refinement and accurately choose the parameters to refine. We try as much as possible to avoid refining unnecessary parameters. In summary, the refinement involves the following steps (see also Appendix 2):

• • Beam intensity and backgrounds. We refine only beam intensity as we use an interpolated background.

• • Cell parameters. Ferropericlase is cubic, so we need to refine only the unit-cell parameter a.

• • Texture. As seen in Figure 10 the texture is fairly strong, thus we refine the texture early. With the E-WIMV method, we obtain first an OD without any sample symmetry to check and validate our hypothesis of imposing an axial symmetry [Figure 10(a)]. The pole figures look fairly symmetrical, even though only a single image with four diffraction peaks was recorded [Figure 8(d)]. This is because of the high cubic crystal symmetry that imposes constraints due to equivalent poles [three for (100), six for (110), and four for (111)]. For lower crystal symmetry, this would be much less complete. Once we verify that the texture and sample orientation is compatible with axial symmetry, we impose “fiber” sample symmetry [Figure 10(b)]. This greatly improves the effective pole figure coverage.

• • Crystallite size and r.m.s. microstrain. Here we assume isotropic crystallite size and microstrain, which results in two refinable parameters. As mentioned earlier, with the coarse-grained LaB₆ standard, it was difficult to refine an accurate instrumental peak broadening. Thus obtained parameter values should be viewed as only qualitative.

• • Stress models. For “Moment pole stress” we start with the elastic tensor values for ferropericlase at atmospheric pressure with C ₁₁ = C ₂₂ = C ₃₃ = 279.5 GPa, C ₁₂ = C ₁₃ = C ₂₃ = 102.2 GPa, C ₄₄ = C ₅₅ = C ₆₆ = 142 GPa, with all others equal to zero (Marquardt et al., Reference Marquardt, Speziale, Reichmann, Frost and Schilling2009) and we refine only the σ₁₁ macrostress value. As an alternative for the “Radial Diffraction in the DAC” model, we refine Q(hkl) factors of each diffraction peak in the refinement range (four parameters).

• • Beam center. If reflection positions are not fitting well with the stress model and one still observes variations of peak position with angle η, refine the detector center errors (two parameters, x and y), since it may have changed during DAC positioning. In our case, it was not necessary.

• • Tilt of the DAC cell. If there is evidence that the compression direction is tilted (not in this case), then we need to correct for this. In the “Radial Diffraction in the DAC” model, it is accomplished by refining the “Alpha” and “Beta” angles for a better fit. In the other stress-based models, the only option is to refine the sample orientation angles that define the coordinate system.

• • Heterogeneities of strain in the DAC cell. In the “Plot 2D” display one may observe asymmetry in the texture between the lower and the upper half of the measured patterns display, while refined patterns demonstrate perfect symmetry. This may be due to heterogeneities of the sample in the DAC, e.g. some grains in the periphery of the cell are subjected to lower pressures and deviatoric stress. To accommodate this, one can use for the last refinement cycle only one half of the diffraction image. However, if only half the Debye ring is used, one should be sure to fix beam center and tilt parameters. Since axial symmetry of texture and stress state is imposed, the entire diffraction image is not needed to derive a reasonably accurate OD.

Figure 10.

Texture information for ferropericlase at 39.6 GPa represented as pole figures (a, b) and inverse pole figures (c). (a) Pole figures without imposing sample symmetry. (b) Pole figures imposing fiber symmetry. (c) Inverse pole figure of the compression direction plotted by BEARTEX. Equal area projection, contours in multiples of a random distribution.

At the end of the analysis the refined cell parameter is 3.9866(1) Å and the corresponding volume is ≈ 63.36 Å³. For radial diffraction the lattice parameter represents the strain resulting from the hydrostatic (pressure) component of the stress tensor. The derived pressure is ≈ 39.6 GPa and the final elastic tensor is C ₁₁ = C ₂₂ = C ₃₃ ≈ 624.4 GPa, C ₁₂ = C ₁₃ = C ₂₃ ≈ 171.1 GPa, and C ₄₄ = C ₅₅ = C ₆₆ ≈ 175.3 GPa; the deviatoric macrostress σ₁₁ component is ≈1.80(1) GPa. To calculate the equivalent t value in Eq. (1) we multiply by 3 this value to obtain 5.4 GPa.

In this analysis, we have been mainly concerned with preferred orientation, which, for axially symmetric textures, is conveniently displayed as inverse pole figures that represent the probability of the fiber axis relative to crystal coordinates. Figure 10(c) is the inverse pole figure of the compression direction after processing with BEARTEX. The texture is moderate, with a pole density maximum of ≈ 2.65 multiples of a random distribution, located close to 001 [Figure 10(d)], as previously observed (e.g., Merkel et al., Reference Merkel, Wenk, Shu, Shen, Gillet, Mao and Hemley2002; Kunz et al., Reference Kunz, Caldwell, Miyagi and Wenk2007; Lin et al., Reference Lin, Wenk, Voltolini, Speziale, Shu and Duffy2009; Kaercher et al., Reference Kaercher, Speziale, Miyagi, Kanitpanyacharoen and Wenk2012). Quantitative texture information for the two models is summarized in Table III.

Table III.

Texture information for ferropericlase at 39.6 GPa; pole densities of different pole figures and inverse pole figure (IPF) in m.r.d. Numbers in parentheses are after exporting the ODF to BEARTEX.