Atom Probe Tomography Analysis of Exsolved Mineral Phases

Environment

Your institution must subscribe to JoVE's Environment section to access this content.

Fill out the form below to receive a free trial or learn more about access:

 

Summary

Analysis of the morphology, composition, and spacing of exsolution lamellae can provide essential information to understand geological processes related to volcanism and metamorphism. We present a novel application of APT for the characterization of such lamellae and compare this approach to the conventional use of electron microscopy and FIB-based nanotomography.

Cite this Article

Copy Citation | Download Citations | Reprints and Permissions

Genareau, K., Perez-Huerta, A., Laiginhas, F. Atom Probe Tomography Analysis of Exsolved Mineral Phases. J. Vis. Exp. (152), e59863, doi:10.3791/59863 (2019).

Abstract

Element diffusion rates and temperature/pressure control a range of fundamental volcanic and metamorphic processes. Such processes are often recorded in lamellae exsolved from host mineral phases. Thus, the analysis of the orientation, size, morphology, composition and spacing of exsolution lamellae is an area of active research in the geosciences. The conventional study of these lamellae has been conducted by scanning electron microscopy (SEM) and transmission electron microscopy (TEM), and more recently with focused ion beam (FIB)-based nanotomography, yet with limited chemical information. Here, we explore the use of atom probe tomography (APT) for the nanoscale analysis of ilmenite exsolution lamellae in igneous titanomagnetite from ash deposits erupted from the active Soufrière Hills Volcano (Montserrat, British West Indies). APT allows the precise calculation of interlamellar spacings (14–29 ± 2 nm) and reveals smooth diffusion profiles with no sharp phase boundaries during the exchange of Fe and Ti/O between the exsolved lamellae and the host crystal. Our results suggest that this novel approach permits nanoscale measurements of lamellae composition and interlamellar spacing that may provide a means to estimate the lava dome temperatures necessary to model extrusion rates and lava dome failure, both of which play a key role in volcanic hazard mitigation efforts.

Introduction

The study of chemical mineralogy has been a major source of information within the field of Earth Sciences for more than a century, as minerals actively record geological processes during and after their crystallization. Physio-chemical conditions of these processes, such as temperature changes during volcanism and metamorphism, are recorded during mineral nucleation and growth in the form of chemical zonation, striations, and lamellae, among others. Exsolution lamellae form when a phase unmixes into two separate phases in the solid state. The analysis of the orientation, size, morphology, and spacing of such exsolution lamellae can provide essential information to understand temperature and pressure changes during volcanism and metamorphism1,2,3 and the formation of ore mineral deposits4.

Traditionally, the study of exsolution lamellae was conducted with the observation of micrographs by simple scanning electron imaging5. More recently, this has been substituted by the use of energy-filtered transmission electron microscopy (TEM) providing detailed observations at the nanoscale level1,2,3. Nevertheless, in both cases, the observations are made in two dimensions (2D), which is not fully adequate for three dimensional (3D) structures represented by these exsolution lamellae. Nanotomography6 is emerging as a new technique for the 3D observation of nanoscale features inside minerals grains, yet there is insufficient information about the composition of these features. An alternative to these approaches is the use of atom probe tomography (APT), representing the highest spatial resolution analytical technique in existence for the characterization of materials7. The strength of the technique lies in the possibility of combining a 3D reconstruction of nanoscale features with their chemical composition at the atomic scale with a near part-per-million analytical sensitivity7. Previous applications of APT to the analysis of geological samples have provided excellent results8,9,10,11, particularly in the chemical characterization of element diffusion and concentrations9,12,13. Yet, this application has not been used for the study of exsolution lamellae, abundant in some minerals hosted in metamorphic and igneous rocks. Here, we explore the use of APT, and its limitations, for the analysis of the size and composition of exsolution lamellae, and interlamellar spacing in volcanic titanomagnetite crystals.

Subscription Required. Please recommend JoVE to your librarian.

Protocol

1. Sourcing, selection, and preparation of mineral grains

NOTE: Samples were obtained from the catalogued collection at the Montserrat Volcano Observatory (MVO) and derived from falling deposits originating from a vigorous ash venting episode at Soufrière Hills Volcano that occurred on 5 October, 2009; this was one of 13 similar events over a course of three days14. This ash venting preceded a new phase of lava dome growth (phase 5) that commenced on 9 October. Previous analysis of this sample showed it to be a combination of dense dome rock fragments, glassy particles, and accidental lithics14.

  1. Pour 1 g of volcanic ash sample into a 10 cm diameter glass Petri dish.
  2. Wrap a small (3 cm x 3 cm) sheet of weighing paper around a 10 G magnet.
  3. Use a paper-wrapped magnet to pull magnetite-rich grains between 100 µm and 500 μm in diameter from the ash sample and place in a 32 μm (5 φ), 8 cm diameter stainless-steel sieve.
  4. Rinse in deionized water for 20–30 s using a squeeze bottle to remove smaller, adhering ash particles (which will pass through the sieve), and air-dry for 24 h.
  5. Affix clean and dry ash particles to sample mounts suitable for the secondary electron microscope (SEM). Image in secondary electron mode at a 15–20 kV accelerating voltage and at a working distance of 10 mm to select the 5–10 best candidates for further analysis. Selected grains should be predominantly (>50%) magnetite (Figure 1a,b).
  6. Affix selected ash grains to clear tape, surround with one-inch diameter hollow mold (metal, plastic, or rubber) that has been internally coated with vacuum grease, and pour in epoxy resin to fill the mold (2 cm3). Allow epoxy to cure according to the specific epoxy instructions.
  7. Once epoxy has cured, remove from mold and peel tape from the bottom. Ash grains should be partially exposed.
  8. Polish the epoxy-cast ash grains using SiC grinding paper of five different grit sizes (400, 800, 1200, 1500 and 2000 grit).
    1. Polish the sample with each grit size, from highest (400) to lowest (2000) in a figure eight motion for at least 10 min. In between grit sizes, sonicate the sample in a bath of deionized water for 10 min.
    2. Check the sample under a microscope to ensure that the polishing grit is not present, and the sample surface is free from scratches. If scratches are present, repeat the polishing procedure with the previous grit size before sonicating and moving to the next grit size.
  9. Polish the epoxy-cat ash grains with alumina polishing suspensions of 1.0 μm and then 0.3 µm on polishing cloths.
    1. Polish the sample with each suspension in a figure eight motion for at least 10 min. In between suspension sizes, sonicate the sample in a bath of deionized water for 10 min.
    2. Check the sample under a microscope to ensure that the suspension is not present and the sample surface is free of scratches. If scratches are present, repeat the polishing procedure with the previous suspension before sonicating and moving to the next suspension size. At the end of the polishing procedure, the epoxy surface should be smooth and the ash grains should be flat and well-exposed.
  10. Coat the sample surface with a conducting coat of ~10 nm thick carbon using an available sputter coating device.
  11. Obtain backscattered electron images of the ash grains with the electron microscope at a 15–20 kV accelerating voltage and a working distance of 10 mm to determine the location of exsolution lamellae in the magnetite (Figure 1c), as conducted in previous studies5.

Figure 1
Figure 1: Example of magnetite-rich ash grains from venting episodes at the Soufrière Hills volcano. (a, b): Backscattered electron images (BSE) of both reacted and unreacted textures in magnetite grains. (c) BSE image of a polished magnetite grain showing the presence of exsolution lamellae (light grey laths; red arrows) of potential ilmenite composition. (d) Secondary electron image of a polished magnetite grain prepared for atom probe tomography (APT) analysis, showing the location of some exsolution lamellae (dashed red lines), which are distributed all along the grain surface, and the location of the wedge extraction (blue arrow). Please click here to view a larger version of this figure.

2. Atom probe tomography (APT) sample preparation

  1. APT samples will be prepared from a wedge of material that reveals the presence of exsolution lamellae (Figure 1d) employing a FIB-based lift-out protocol16 (Figure 2). Prior to FIB work, sputter coat the sample surface with 15 nm layer of Cu to avoid electron charging and sample drifting.
  2. Using a focused ion beam in a dual beam scanning electron microscope (FIB-SEM), deposit a rectangle of platinum (Pt) (3 μm in thickness) on the polished section of interest containing the lamellae over a 1.5 µm x 20 µm region using a gallium (Ga+) ion beam at 30 kV and 7 pA.
    NOTE: This platinum layer is deposited to protect the region of interest (ROI) from ion beam damage.
  3. Mill three wedges of material below three sides of the Pt rectangle using the ion beam (30 kV, 1 nA). See Figure 1d and Figure 2.
  4. Insert the gas injection system (GIS) and weld the wedge to an in situ nano-manipulator using GIS-deposited Pt before cutting the final edge free (Figure 2a).
  5. Using the Ga+ ion beam (5 kV and 240 pA), cut ten 1–2 μm wide segments from the wedge and sequentially affix them with Pt to the tops of Si posts of a microtip array coupon (Figure 2b–d).
  6. Shape and sharpen each specimen tip using annular milling patterns of increasingly smaller inner and outer diameters (Figure 3). Initially, perform the milling at 30 kV to produce the specimen geometry necessary for APT (Figure 3, left panel).
  7. Perform the final milling at an accelerating voltage of 5 kV in order to reduce Ga+ implantation and obtain a consistent tip-to-tip shape (Figure 3, right panel).
  8. By applying the measuring tools of the SEM to the figure, ensure that the diameter at the top of the tips ranges 50–65 nm, while the shank angle of the tips ranges from 25° to 38°.
    NOTE: Further details have been previously published, describing the conventional lift-out protocol16.

Figure 2
Figure 2: Example of FIB-SEM sample preparation protocol for APT analysis. (a) Wedge (W) lift-out extraction with the nanomanipulator (Nm). (b) Lateral view of the micro-coupon array of silicon posts mounted on a copper clip. (c) Top view of the micro-coupon array of silicon posts showing the nanomanipulator for mounting the wedge sections. (d) Wedge fragment (S), showing a portion of the protective platinum cap (Ptc), mounted on a silicon post after welding with platinum (Ptw). Please click here to view a larger version of this figure.

Figure 3
Figure 3: Example of tips prepared for APT analysis. (Left) Image of tip after the first stage of sharpening. (Right) Image of the same tip after low kV cleaning, indicating the tip radius (67.17 nm) and the shank angle (26°). Please click here to view a larger version of this figure.

3. APT data acquisition

  1. Perform analysis with a local electrode atom probe (LEAP) equipped with a pico-second 355 nm UV laser. See specific LEAP running parameters in Table 1.
    NOTE: Analyses were performed with a LEAP equipped with a pico-second 355 nm UV laser, housed in the Central Analytical Facility (CAF) at The University of Alabama.
  2. Mount the micro-coupon with the sharpened tips, welded to the Si posts, in a specimen puck and load into a carousel for placement inside the LEAP.
  3. Insert the carousel inside the buffer chamber of the LEAP.
  4. Turn the laser head on and perform a laser calibration.
  5. After achieving vacuum in the analysis chamber at or below 6 x 10-11 Torr, insert the puck specimen into the main analysis chamber. For this use a transfer rod; this is operated with a series of automatic steps and manual insertion.
  6. Before analysis, select the tip by moving the specimen puck to align the micro-coupon with the local electrode and update the database to indicate the tip number.
    NOTE: Four out of six tips were analyzed successfully (two fractured during analysis) and resulted in a variable amount of acquired data ranging from 26 to 92 million total detected ions, which corresponded to the removal of a 160–280 nm-thick layer of magnetite (see specific LEAP running parameters in Table 1).
Specimen 207 217 218 219
Sample Description SHV Magnetite SHV Magnetite SHV Magnetite SHV Magnetite
Instrument Model LEAP 5000 XS LEAP 5000 XS LEAP 5000 XS LEAP 5000 XS
Instrument Settings
Laser Wavelength 355 nm 355 nm 355 nm 355 nm
Laser Pulse Rate 60 pJ 30 pJ 30 pJ 30 pJ
Laser Pulse Energy 500 kHz 500 kHz 500 kHz 500 kHz
Evaporation Control Detection Rate Detection Rate Detection Rate Detection Rate
Target Detection Rate (%) 0.5 0.5 0.5 0.5
Nominal Flight Path (mm) 100 100 100 100
Temperature (K) 50 50 50 50
Pressure (Torr) 5.7x10-11 6.0x10-11 6.1x10-11 6.1x10-11
ToF offset, to (ns) 279.94 279.94 279.94 279.94
Data Analysis
Software IVAS 3.6.12 IVAS 3.6.12 IVAS 3.6.12 IVAS 3.6.12
Total Ions: 26,189,967 92,045,430 40,013,656 40,016,543
Single 15,941,806 55,999,564 24,312,784 23,965,867
Multiple 9,985,564 35,294,528 15,331,670 15,716,119
Partial 262,597 751,338 369,202 334,557
Reconstructed Ions: 25,173,742 89,915,256 38,415,309 39,120,141
Ranged 16,053,253 61,820,803 25,859,574 26,598,745
Unranged 9,120,489 28,094,453 12,555,735 12,521,396
Background (ppm/nsec) 12 12 12 12
Reconstruction
Final tip state Fractured Fractured Fractured Fractured
Pre-/Post-analysis Imaging SEM/n.a. SEM/n.a. SEM/n.a. SEM/n.a.
Radius Evolution Model “voltage” “voltage” “voltage” “voltage”
Vinitial; Vfinal 2205 V; 6413 V 2361 V; 7083 V 2198 V; 6154 V 2356 V; 6902 V

Table 1. Atom probe tomography data acquisition settings and run summary.

4. APT data processing

  1. Open the dataset in the processing software (see the Table of Materials) and perform the following steps for data analysis.
    1. Review the information setup.
    2. Select ion sequence range based on the voltage history plot. Select the detector region of interest (ROI).
    3. Perform time-of-flight (TOF) correction. Use peaks corresponding to oxygen and iron for the TOF correction.
    4. Perform mass calibration with the identification of main peaks.
    5. Perform the ranging of ions for their assignments to specific masses.
    6. Perform the reconstruction of the tip profile.
  2. Show the data into the two main formats: 1) mass-to-charge state ratio (Da) chemical spectra (Figure 4); and 2) 3D reconstructions of tip specimens (Figure 5).
  3. Define peak ranges as the entire visible peak, or adjust manually when large thermal tails are present, for each mass-to-charge state ratio spectrum (Figure 4). These peaks represent single elements or molecular species, and the decomposition of peaks provides the overall chemical composition for each tip or feature (i.e., clusters and exsolution lamellae) inside each tip (Table 2).
  4. Perform three-dimensional (3D) tip reconstructions using the “voltage” tip profile method17 to determine the reconstructed radius as a function of analyzed depth (Figure 5 and Movie 1).
  5. Reconstruct isosurfaces of exsolution lamellae to conduct interlamellar spacing measurements (Figure 5) and establish the host mineral-lamella chemical relationship using proxigrams17,18 (Figure 6).
  6. Measure interlamellar spacings with image analysis software.

Figure 4
Figure 4: Example of a representative APT mass-to-charge spectrum. Spectrum for the analyzed magnetite crystal with individual ranged peaks showing examples of the identification of peaks corresponding to single elements (e.g., oxygen (O) or iron (Fe)) or molecules (e.g., FeO). Please click here to view a larger version of this figure.

Specimen 207 217 218 219
Element Atom count Atomic % 1s error Atom count Atomic % 1s error Atom count Atomic % 1s error Atom count Atomic % 1s error
O 9459276 40.263 0.0155 36679256 40.724 0.0080 15396155 41.010 0.0124 16212281 41.224 0.0122
Fe 9424298 40.114 0.0155 35948593 39.913 0.0079 14829905 39.502 0.0121 15006853 38.159 0.0116
Mn 15954 0.068 0.0005 72884 0.081 0.0003 28166 0.075 0.0004 31450 0.080 0.0005
Mg 123755 0.527 0.0015 486732 0.540 0.0008 203596 0.542 0.0012 234231 0.596 0.0012
Al 85598 0.364 0.0013 329602 0.366 0.0006 134637 0.359 0.0010 154779 0.394 0.0010
Si 13855 0.059 0.0005 39307 0.044 0.0002 16278 0.043 0.0003 25750 0.065 0.0004
Na 166 0.001 0.0001 1254 0.001 0.0000 447 0.001 0.0001 1468 0.004 0.0001
Ti 4360052 18.558 0.0097 16478946 18.296 0.0049 6920481 18.434 0.0076 7645849 19.442 0.0077
H 10657 0.045 0.0004 30522 0.034 0.0002 12899 0.034 0.0003 14478 0.037 0.0003
Total 23493611 100.00 0.04 90067097 100.00 0.02 37542563 100.00 0.04 39327140 100.00 0.03
Fe+Ti+O 98.94 98.93 98.95 98.82
Fe/Ti 2.16 2.18 2.14 1.96

Table 2. Atom probe tomography bulk compositional data for all analyzed specimens.

Subscription Required. Please recommend JoVE to your librarian.

Representative Results

Like many titanomagnetite crystals from various stages of the Soufrière Hills Volcano (SHV) eruption, the crystal analyzed here contains exsolution lamellae <10 µm in thickness, visible in secondary SEM images (Figure 1d), which separate zones of Ti-rich magnetite, indicating a C2 stage of oxidation18. Based upon the SEM images, spacing between these lamellae ranges from 2 to 6 µm (n = 15). Four titanomagnetite specimen tips, referred as 207, 217, 218, and 219, were successfully extracted from this single crystal and analyzed by APT (Figure 5). Two of the specimens (207 and 218) showed homogenous concentrations of both Fe and Ti throughout (Figure 5a), indicating that lamellae were not intersected. The other two specimens (217 and 219) showed zones with variable concentrations in Fe, O, and Ti (Figure 5b-e). These features are parallel to each other and have tapered terminations, indicative of trellis ilmenite18. Specimen 219 contains a larger proportion of the intersected lamellae than specimen 217. 3D reconstructions of the APT data (Figure 5c-e, Movie 1) permit a precise measurement of the interlamellar spacing (λ) and provide length scales that average 29 nm for specimen 219 (n = 30) and 14 nm for specimen 217 (n = 15), with a 1s value of 2 nm for both. In addition to these measurements, APT permits extraction of chemical information across these lamellae at high spatial resolution (nanoscale) through the analysis of proxigrams, taking the point 0 as the intersection between the lamella and the host mineral (Figure 6). Proxigram diffusion profiles through these zones are smooth. Atomic concentrations of Ti in the crystal, 17% in specimen 217 and 16.5% in specimen 219 (Figure 6), confirm that it is a titanomagnetite and are consistent with previous petrologic analyses of SHV eruptive products18. These proxigrams also confirm that the composition of lamellae matches that of ilmenite (Figure 6).

Figure 5
Figure 5: Example of 3D atomic reconstructions of magnetite tips analyzed (z values in nm). (a) Specimen 218, showing homogenous concentrations of O, Fe, and Ti. (b) Specimen 219, displaying regions depleted in Fe and enriched in O and Ti (lighter areas). (c) Elemental isoconcentration surfaces of specimen 219, showing intralamellar concentrations of Fe < 30.0% in blue, Ti > 25.0% in yellow, and O < 51.5% in purple. (d) View of same area in panel c, but rotated 90° to reveal the measured lamellar spacing (l). (e) Specimen 217, showing a relatively smaller portion of exsolution lamellae in the lower left (intralamellar concentrations: Fe < 19.0%, Ti > 33.0%, O < 49.0%). Please click here to view a larger version of this figure.

Figure 6
Figure 6: Proxigrams of APT data showing atomic concentrations of O, Fe and Ti in specimens 217 and 219, respectively. A distance of zero on the x-axis (dashed vertical line) represents the boundary between the titanomagnetite on the left and the ilmenite lamellae on the right. Across this boundary, Ti concentrations increase from 17.0% to 44.0% and from 16.5% to 42.5% in specimens 217 and 219, respectively. Fe contents decrease from 37.7% to 0.8% and from 38.5% to 0.6% in specimens 217 and 219, respectively. O concentrations increase from 40.0% to 50.2% and from 38.8% to 50.6% in specimens 217 and 219, respectively. Ti and O diffuse toward the lamellae (to the right) and Fe is diffusing away from the lamellae (to the left). Error in all measurements is < 2 atomic %. Please click here to view a larger version of this figure.

Movie 1. 3D elemental isoconcentration reconstruction of specimen 219, showing intralamellar concentrations of Fe < 30.0% in blue, Ti > 25.0% in yellow, and O < 51.5% in purple, and rotated 360° along the longitudinal (z) axis. Please click here to download this file.

Subscription Required. Please recommend JoVE to your librarian.

Discussion

3D APT data reconstructions allow a precise measurement of the interlamellar spacing in the analyzed crystal at a resolution three orders of magnitude higher than those measured from conventional SEM images. This indicates that atomic variations in chemistry occur over a spatial extent three orders of magnitude smaller than optically observable mineralogical changes. Also, the measured interlamellar distances (29 nm and 14 nm), are consistent with the length scale for oxyexsolution as opposed to that for nucleation and growth of a separate phase, the latter of which occurs over length scales an order of magnitude greater19,20. Oxyexsolution of the titanomagnetite examined here may have resulted from either heating of the magma within the chamber due to mingling events, or oxidation induced by atmospheric exposure during ascent through the conduit and emplacement at the vent. The titanomagnetite crystal used in this study displays numerous lamellae on the order of 10 µm or less in diameter, indicating sufficient time for partial exsolution of the entire 0.06 mm2 crystal. That observation, in conjunction with the ash-venting origin of the sample, suggests that the lamellae were formed from oxidation of the lava dome following emplacement at the vent.

Figure 7
Figure 7: Schematic representation of different possibilities for capturing exsolution lamellae in APT tips, and the implications for measuring lamellar spacing (λ). Please click here to view a larger version of this figure.

These measurements of the interlamellar spacing were only possible in two of the four tips analyzed and this sampling bias could induce error. As we only analyze nanoscale volumes of the crystals, each tip could capture partial representation of the distribution of lamellae, potentially leading to an erroneous calculation of interlamellar spacing (λ) (Figure 7). Nevertheless, with the analysis of sufficient tips and the 3D tomography capabilities of APT, our approach provides a novel method to precisely measure λ, which can be fundamental to understand a variety of igneous and metamorphic processes. For example, analysis of Fe-Ti diffusion in magnetite crystals has been used to characterize magma mingling events and changes in magma temperature at Soufrière Hills Volcano19. The interdiffusion rate of Fe and Ti could be modeled from accurate measurements of the interlamellar spacing if the timescale of diffusion can be constrained. Previous studies have utilized exsolution lamellae to deduce cooling rates in igneous intrusions21,22, and the novel approach of using APT can potentially be utilized to constrain element interdiffusion and improve calculations of magma and lava dome temperatures in active volcanic systems23,24. Besides the precise measurement of 3D structures at nanoscale, APT provides chemical information at the atomic scale for the same spatial resolution. This has resulted in demonstrating that the transition from titanomagnetite to ilmenite is gradual and smooth (Figure 6). This is in contrast to previous studies suggesting sharp and distinct contacts between the exsolving lamellae and the host phase, based on microscopy observations (SEM and TEM) without the chemical information. Consequently, only the addition of APT can accurately provide the geochemical characteristics of these phase transitions.

Atom probe tomography (APT) is still an emerging technique for geological applications25, yet our case study demonstrates the usefulness of applying this approach for the study of exsolution lamellae, quite common in minerals hosted in igneous and metamorphic rocks. In particular for understanding volcanic processes, future studies can examine multiple samples with exsolution lamellae throughout lava domes (derived from either ash venting episodes or dome collapse events) in order to better constrain variations in temperature during eruptive episodes with calculated diffusion rates.

Subscription Required. Please recommend JoVE to your librarian.

Disclosures

The authors have nothing to disclose.

Acknowledgments

This work was supported by funding from the National Science Foundation (NSF) through grants EAR-1560779 and EAR-1647012, the Office of the VP for Research and Economic Development, the College of Arts and Sciences, and the Department of Geological Sciences. Authors also acknowledge Chiara Cappelli, Rich Martens and Johnny Goodwin for technical assistance and the Montserrat Volcano Observatory for providing the ash samples.

Materials

Name Company Catalog Number Comments
InTouchScope Secondary Electron Microscope (SEM) JEOL JSM-6010PLUS/LA
Focus Ion Beam (FIB) Secondary Electron Microscope (SEM) TESCAN LYRA XMU
Local Electrode Atom Probe (LEAP) CAMECA 5000 XS
Integrated Visualization and Analysis Software (IVAS, version 3.6.12). processing software

DOWNLOAD MATERIALS LIST

References

  1. Kasama, T., Golla-Schindler, U., Putnis, A. High-resolution and energy-filtered TEM of the interface between hematite and ilmenite exsolution lamellae: Relevance to the origin of lamellar magnetism. American Mineralogist. 88, 1190-1196 (2003).
  2. Hofer, F., Wabichler, P., Grogger, W. Imaging of nanometer-sized precipitates in solids by electron spectroscopic imaging. Ultramicroscopy. 59, 15 (1995).
  3. Golla, U., Putnis, A. Valence state mapping and quantitative electron spectroscopic imaging of exsolution in titanohematite by energy-filtered TEM. Physics and Chemistry of Minerals. 28, 119-129 (2001).
  4. Wang, R. C., et al. Cassiterite exsolution with ilmenite lamellae in magnetite from the Huashan metaluminous tin granite in southern China. Mineralogy and Petrology. 71-84 (2012).
  5. Robinson, P., Gordon, L., Nord, M. R., Smyth, J. R., Jaffe, H. W. Exsolution lamellae in augite and pigeonite: fossil indicators of lattice parameters at high temperature and pressure. American Mineralogist. 62, 857-873 (1977).
  6. Austrheim, H., et al. Fragmentation of wall rock garnets during deep crustal earthquakes. Science Advances. 3, (2017).
  7. Kelly, T. F., Larson, D. J. Atom probe tomography 2012. Annual Review of Materials Research. 42, 1-31 (2012).
  8. Gordon, L. M., Joester, D. Nanoscale chemical tomography of buried organic-inorganic interfaces in the chiton tooth. Nature. 469, 194-197 (2011).
  9. Valley, J. W., et al. Hadean age for a post-magma-ocean zircon confirmed by atom-probe tomography. Nature Geoscience. 7, 219-223 (2014).
  10. Pérez-Huerta, A., Laiginhas, F., Reinhard, D. A., Prosa, T. J., Martens, R. L. Atom probe tomography (APT) of carbonate minerals. Micron. 80, 83-89 (2016).
  11. Weber, J., et al. Nano-structural features of barite crystals observed by electron microscopy and atom probe tomography. Chemical Geology. 51-59 (2016).
  12. Fougerouse, D., et al. Nanoscale gold clusters in arsenopyrite controlled by growth rate not concentration: Evidence from atom probe microscopy. American Mineralogist. 101, 1916-1919 (2016).
  13. Peterman, E. M., et al. Nanogeochronology of discordant zircon measured by atom probe microscopy of Pb-enriched dislocation loops. Science Advances. 2, (2016).
  14. Cole, P. D., et al. Ash venting occurring both prior to and during lava extrusion at Soufriere Hills Volcano, Montserrat, from 2005 to 2010. Geological Society, London, Memoirs. 39, 71-92 (2014).
  15. Thompson, G. B., et al. In situ site-specific specimen preparation for atom probe tomography. Ultramicroscopy. 107, 131-139 (2007).
  16. Haggerty, S. E. Oxide textures; a mini-atlas. Reviews in Mineralogy and Geochemistry. 25, 129-219 (1991).
  17. Gault, B., Moody, M. M., Cairney, J. M., Ringer, S. P. Atom Probe Microscopy. Springer Series in Material Sciences. 160, (2012).
  18. Larson, D. J., Prosa, T. J., Ulfig, R. M., Geiser, B. P., Kelly, T. F. Local Electrode Atom Probe Tomography: A User’s Guide. Springer. New York. 318 (2013).
  19. Devine, J. D., Rutherford, M. J., Norton, G. E., Young, S. R. Magma storage region processes inferred from geochemistry of Fe–Ti oxides in andesitic magma, Soufriere Hills Volcano. Journal of Petrology. 44, Montserrat, WI. 1375-1400 (2003).
  20. Jackson, M., Bowles, J. A. Curie temperatures of titanomagnetite in ignimbrites: Effects of emplacement temperatures, cooling rates, exsolution, and cation ordering. Geochemistry, Geophysics, Geosystems. 15, 4343-4368 (2014).
  21. Harrison, R. J., Putnis, A. The magnetic properties and crystal chemistry of oxide spinel solid solutions. Surveys in Geophysics. 19, 461-520 (1998).
  22. Price, G. D. Microstructures in titanomagnetites as guides to cooling rates of a Swedish intrusion. Geological Magazine. 116, 313-318 (1979).
  23. Price, G. D. Exsolution in titanomagnetites as an indicator of cooling rates. Mineralogical Magazine. 46, 19-25 (1982).
  24. Kuhlman, K. R., Martens, R. L., Kelly, T. F., Evans, N. D., Miller, M. K. Fabrication of specimens of metamorphic magnetite crystals for field ion microscopy and atom probe microanalysis. Ultramicroscopy. 89, 169-176 (2001).
  25. Dégi, J., Abart, R., Török, K., Rhede, D., Petrishcheva, E. Evidence for xenolith–host basalt interaction from chemical patterns in Fe–Ti-oxides from mafic granulite xenoliths of the Bakony–Balaton Volcanic field (W-Hungary). Mineralogy and Petrology. 95, 219-234 (2009).
  26. Saxey, D. W., Moser, D. E., Piazolo, S., Reddy, S. M., Valley, J. W. Atomic worlds: Current state and future of atom probe tomography in geoscience. Scripta Materialia. 148, 115-121 (2018).

Comments

0 Comments


    Post a Question / Comment / Request

    You must be signed in to post a comment. Please or create an account.

    Usage Statistics