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Journal articles on the topic 'Geochronology'

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Published: 4 June 2021

Last updated: 30 July 2024

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1

Bowring, Samuel A., Blair Schoene, James L. Crowley, Jahandar Ramezani, and Daniel J. Condon. "High-Precision U-Pb Zircon Geochronology and the Stratigraphic Record: Progress and Promise." Paleontological Society Papers 12 (October 2006): 25–45. http://dx.doi.org/10.1017/s1089332600001339.

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High-precision geochronological techniques have improved in the past decade to the point where volcanic ash beds interstratified with fossil-bearing rocks can be dated to a precision of 0.1% or better. The integration of high-precision U-Pb zircon geochronology with bio/chemo-stratigraphic data brings about new opportunities and challenges toward constructing a fully calibrated time scale for the geologic record, which is necessary for a thorough understanding of the distribution of time and life in Earth history. Successful implementation of geochronology as an integral tool for the paleontologist relies on a basic knowledge of its technical aspects, as well as an ability to properly evaluate and compare geochronologic results from different methods. This paper summarizes the methodology and new improvements in U-Pb zircon geochronology by isotope dilution thermal ionization mass spectrometry, specifically focused on its application to the stratigraphic record.

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2

Ferrusquia-Villafranca, Ismael. "Do GSSPs render dual time-rock/time classification and nomenclature redundant?" Stratigraphy 6, no. 2 (2009): 135–69. http://dx.doi.org/10.29041/strat.06.2.07.

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The Geological Society of London Proposal for "...ending the distinction between the dual stratigraphic terminology of time-rock units (of chronostratigraphy) and geologic time units (of geochronology). The long held, but widely misunderstood distinction between these two essentially parallel time scales has been rendered unnecessary by the adoption of the global stratotype sections and points (GSSP-golden spike) principle in defining intervals of geologic time within rock strata." Our review of stratigraphic principles, concepts, models and paradigms through history clearly shows that the GSL Proposal is flawed and if adopted will be of disservice to the stratigraphic community. We recommend the continued use of the dual stratigraphic terminology of chronostratigraphy and geochronology for the following reasons: (1) time-rock (chronostratigraphic) and geologic time (geochronologic) units are conceptually different; (2) the subtended time-rock's unit space between its "golden spiked-marked" lower and upper boundaries, actually corresponds to the duration of the time-rock unit's defining geologic s.l. events-set; therefore, in no way can physical time (instants or intervals) be directly defined by GSSPs, (3) combining in a single system of "chronostratigraphic units" the time-rock and geologic time units as currently understood, leads to the epistemological error of uniting evidence (rock successions) with inference (the interpreted duration of chosen defining events); (4) the redundancy of the terms eonothem, erathem, system, series, and stage with eon, era, period, epoch and age lacks support, given that they are conceptually different; in fact, referring to "eon," "era," etc. as terms uniting both time-rock and geochronologic connotations will produce needless nomenclatorial confusion, attaching different meanings to already well known and widely used geologic terms; and (5) the reversion of 'geochronology' to its main stream and original meaning of numerical dating has no foundation, just by considering that the use of geochronolgy precedes numerical dating, which became practical by the 1960's. We endorse the following: (1) the GSSP network needs to be improved through the use of reference sections at high latitude sites, and in sedimentary continental rock successions of achievable, dependable positioning in the global standard timetable; and (2) to attend to researchers using astronomically-forced sedimentary systems, the designation of unit stratotypes needs to be reinstated as a valid and as a, complementary means of defining chronostratigraphic units, particularly at the stage and lower chronostratigraphic rank.

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3

BERGGREN, WILLIAM A., DENNIS V. KENT, JOHN J. FLYNN, and JOHN A. VAN COUVERING. "Cenozoic geochronology." Geological Society of America Bulletin 96, no. 11 (1985): 1407. http://dx.doi.org/10.1130/0016-7606(1985)96<1407:cg>2.0.co;2.

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4

Stern, R. A., I. R. Fletcher, B. Rasmussen, N. J. McNaughton, and B. De Waele. "Nano-geochronology?" Geochimica et Cosmochimica Acta 70, no. 18 (August 2006): A614. http://dx.doi.org/10.1016/j.gca.2006.06.1138.

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5

Cooperdock, Emily H. G., Florian Hofmann, Ryley M. C. Tibbetts, Anahi Carrera, Aya Takase, and Aaron J. Celestian. "Technical note: Rapid phase identification of apatite and zircon grains for geochronology using X-ray micro-computed tomography." Geochronology 4, no. 2 (July 21, 2022): 501–15. http://dx.doi.org/10.5194/gchron-4-501-2022.

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Abstract. Apatite and zircon are among the best-studied and most widely used accessory minerals for geochronology and thermochronology. Given that apatite and zircon are often present in the same lithologies, distinguishing the two phases in crushed mineral separates is a common task for geochronology, thermochronology, and petrochronology studies. Here we present a method for efficient and accurate apatite and zircon mineral phase identification and verification using X-ray micro-computed tomography (microCT) of grain mounts that provides additional three-dimensional grain size, shape, and inclusion suite information. In this study, we analyze apatite and zircon grains from Fish Canyon Tuff samples that went through methylene iodide (MEI) and lithium heteropolytungstate (LST) heavy liquid density separations. We validate the microCT results using known standards and phase identification with Raman spectroscopy, demonstrating that apatite and zircon are distinguishable from each other and other common phases, e.g., titanite, based on microCT X-ray density. We present recommended microCT scanning protocols after systematically testing the effects of different scanning parameters and sample positions. This methodology can help to reduce time spent performing density separations with highly toxic chemicals and visually inspecting grains under a light microscope, and the improved mineral identification and characterization can make geochronologic data more robust.

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6

Smit, Karen V., Suzette Timmerman, Sonja Aulbach, Steven B. Shirey, Stephen H. Richardson, David Phillips, and D. Graham Pearson. "Geochronology of Diamonds." Reviews in Mineralogy and Geochemistry 88, no. 1 (July 1, 2022): 567–636. http://dx.doi.org/10.2138/rmg.2022.88.11.

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7

Mezger, K. "Geochronology and Metamorphism." Mineralogical Magazine 58A, no. 2 (1994): 605–6. http://dx.doi.org/10.1180/minmag.1994.58a.2.51.

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8

De Laeter, J. R., A. J. W. Gleadow, and I. McDougall. "Geochronology in Australia." Australian Journal of Earth Sciences 55, no. 6-7 (August 2008): 721–22. http://dx.doi.org/10.1080/08120090802094077.

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9

Schmitz, M. D., and K. F. Kuiper. "High-Precision Geochronology." Elements 9, no. 1 (February 1, 2013): 25–30. http://dx.doi.org/10.2113/gselements.9.1.25.

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10

Berggren, William A. "Time and time again: getting it right." Paleontological Society Special Publications 6 (1992): 27. http://dx.doi.org/10.1017/s2475262200005876.

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The passage of time cannot be measured in vacuo. Recognition of the time-continuum can only be made by reference to physical and/or biotic events in the geohistorical (rock) record. Inasmuch as these events in the rock record must be measurable in some fashion, they must be related to an objective and retrievable reference standard. Thus the “holy trinity” of litho-bio-and chronostratigraphy can serve as the material (concrete) evidence for the totally conceptual geochronologic units which have no objective existence apart from the natural world.Geochronology is defined here as the conceptual division of continuous time as measured (geochronometry) by the progression in an ordinal series of events. This is best achieved by an approach which integrates four independent data sets: magnetostratigraphy, sea-floor spreading magnetic anomalies, biostratigraphy and isotopic dating. This integrated approach has resulted, until recently, in an ordinal framework capable of measuring the passage of time with greater resolution (precision), though perhaps with less accuracy, than a radiometric approach alone. Recent improvements in the field of isotopic dating-the single crystal laser fusion (SCLF) 40Ar/39Ar technique - now render possible dates with analytical precision of <1% in the early to mid-Cenozoic. The implication for high resolution correlation is clear: until recently biostratigraphy and biochronology have been routinely able to achieve a degree of chronologic resolution considerably higher than that of isotopic dating with its inherently large analytical errors. Laser fusion dating is now capable of providing numerical values for parts of the stratigraphic record with comparable or greater precision than classical biostratigraphy and biochronology. It is clear, now more than ever, that an accurate and precise biostratigraphy is important as we continue to improve upon the geochronologic framework which underlies attempts at high resolution correlation between marginal, platform and deep-sea stratigraphies.A review of the philosophic and methodologic approach of various Cenozoic geochronologic schemes and their strengths and weaknesses will be presented together with a brief discussion of a new, and as yet unpublished, revision to Cenozoic geochronology. Recent assessment of sea floor anomaly patterns indicate a need to stretch the spacing of the interval between anomalies 3A to 5 resulting in an age increase of about 0.5my for Anomaly 5 from 8.92–10.42Ma (BKVC85) to 9.6–11.0Ma; the revised age estimates are consistent with those of McDougall (1984) based on radioisotopic dating of Icelandic basalts. No other major (age) revisions to Neogene chronology are contemplated. However, discrete adjustments are required in the late Neogene as magnetostratigraphic boundaries and biostratigraphic datum events are (re)correlated to the recently proposed astronomically calibrated orbital time scale of Hilgen and Langereis. In the Paleogene the major change is centered on readjustment of the Eocene which, while retaining its relative duration of ~21my, has younger (~34Ma) and older (~54.5Ma) limits, respectively, not unlike some estimates made over 20 years ago. Emphasis on implications for Paleogene geochronology will be stressed with particular reference to events around the Paleocene/Eocene boundary and the integration of correlative NW European and Gulf and Atlantic Coastal Plain stratigraphies in a sequence stratigraphic framework. The continuing efforts being devoted to revising Cenozoic geochronology have as their overiding goal the simple yet scientifically elusive objective of “getting it right”.

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11

Donaghy, Erin E., Michael P. Eddy, Federico Moreno, and Mauricio Ibañez-Mejia. "Minimizing the effects of Pb loss in detrital and igneous U–Pb zircon geochronology by CA-LA-ICP-MS." Geochronology 6, no. 1 (March 27, 2024): 89–106. http://dx.doi.org/10.5194/gchron-6-89-2024.

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Abstract. Detrital zircon geochronology by laser ablation–inductively coupled plasma–mass spectrometry (LA-ICP-MS) is a widely used tool for determining maximum depositional ages and sediment provenance, as well as reconstructing sediment routing pathways. Although the accuracy and precision of U–Pb geochronology measurements have improved over the past 2 decades, Pb loss continues to impact the ability to resolve zircon age populations by biasing affected zircon toward younger apparent ages. Chemical abrasion (CA) has been shown to reduce or eliminate the effects of Pb loss in zircon U–Pb geochronology but has yet to be widely applied to large-n detrital zircon analyses. Here, we assess the efficacy of the chemical abrasion treatment on zircon prior to analysis by LA-ICP-MS and discuss the advantages and limitations of this technique in relation to detrital zircon geochronology. We show that (i) CA does not systematically bias LA-ICP-MS U–Pb dates for 13 reference materials that span a wide variety of crystallization dates and U concentrations, (ii) CA-LA-ICP-MS U–Pb zircon geochronology can reduce or eliminate Pb loss in samples that have experienced significant radiation damage, and (iii) bulk CA prior to detrital zircon U–Pb geochronology by LA-ICP-MS improves the resolution of age populations defined by 206Pb/238U dates (Neoproterozoic and younger) and increases the percentage of concordant analyses in age populations defined by 207Pb/206Pb dates (Mesoproterozoic and older). The selective dissolution of zircon that has experienced high degrees of radiation damage suggests that some detrital zircon age populations could be destroyed or have their abundance significantly modified during this process. However, we did not identify this effect in either of the detrital zircon samples that were analyzed as part of this study. We conclude that pre-treatment of detrital zircon by bulk CA may be useful for applications that require increased resolution of detrital zircon populations and increased confidence that 206Pb/238U dates are unaffected by Pb loss.

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12

Gaynor, Sean P., Joshua H. F. L. Davies, and Urs Schaltegger. "High-Precision Geochronology of LIP Intrusions: Records of Magma–Sediment Interaction." Elements 19, no. 5 (October 1, 2023): 302–8. http://dx.doi.org/10.2138/gselements.19.5.302.

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Reconstructing the tempo and emplacement mechanisms of large igneous provinces (LIPs) and establishing potential links to environmental change and biological crises requires detailed and targeted high-precision geochronology. Contact metamorphism during LIP intrusive magmatism can release large volumes of thermogenic gas, so determining the timing of these events relative to global climate change is crucial. The most reliable age information comes from U-Pb geochronology; however, LIP mafic igneous rocks do not commonly crystallize U-bearing minerals, such as zircon or baddeleyite. Recent work has shown that U-rich minerals can crystallize in fractionated melt pockets in intrusive components of LIPs after contamination of the melt by sedimentary rocks at emplacement level. Zircon and baddeleyite from these pockets make high-precision U-Pb geochronology of LIPs possible, but these unique mechanisms add other complexities.

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13

Corcoran, Loretta, and Antonio Simonetti. "Geochronology of Uraninite Revisited." Minerals 10, no. 3 (February 25, 2020): 205. http://dx.doi.org/10.3390/min10030205.

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Identification of uraninite provenance for the purpose of nuclear forensics requires a multifaceted approach. Various geochemical signatures, such as chondrite normalized rare earth element patterns, help identify and limit the potential sources of uraninite based on the geological setting of the uranium ore mineralization. The inclusion of accurate age determinations to discriminate geochemical signatures for natural uranium ores may help to potentially restrict geographical areas for provenance consideration. Determining a robust age for uraninite formation is somewhat difficult, due to well known, inherent difficulties associated with open system behavior that involve either uranium and/or lead loss or gain. However, open system behavior should not perturb their Pb isotopic compositions to the same degree as Pb isotopes should not fractionate during alteration processes. Here, a suite of pristine and altered samples of uraninite was examined for their Pb isotope compositions, and these yielded geologically meaningful secondary Pb–Pb isochron ages. The degree of alteration within individual uraninite samples, which is extremely variable, does not appear to affect the calculated ages. The approach adopted here yields insightful age information, and hence, is of great value for source attribution in forensic analyses of raw nuclear materials.

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14

SÖDERLUND, Ulf. "Geochronology of Mafic Intrusions." Acta Geologica Sinica - English Edition 90, s1 (October 2016): 83. http://dx.doi.org/10.1111/1755-6724.12901.

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15

Haynes, C. V., and George A. Agogino. "Geochronology of Sandia Cave." Smithsonian Contributions to Anthropology, no. 32 (1986): 1–32. http://dx.doi.org/10.5479/si.00810223.32.1.

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16

Sinton, Christopher W., David M. Christie, and Robert A. Duncan. "Geochronology of Galápagos seamounts." Journal of Geophysical Research: Solid Earth 101, B6 (June 10, 1996): 13689–700. http://dx.doi.org/10.1029/96jb00642.

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17

Barfod, Gry H., Olga Otero, and Francis Albarède. "Phosphate Lu–Hf geochronology." Chemical Geology 200, no. 3-4 (October 2003): 241–53. http://dx.doi.org/10.1016/s0009-2541(03)00202-x.

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18

Lee, James K. W. "Multipath diffusion in geochronology." Contributions to Mineralogy and Petrology 120, no. 1 (May 1995): 60–82. http://dx.doi.org/10.1007/bf00311008.

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19

Moorbath, Stephen. "Geochronology – Aims and reminiscences." Applied Geochemistry 24, no. 6 (June 2009): 1087–92. http://dx.doi.org/10.1016/j.apgeochem.2009.02.008.

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20

Cooper, J. A., J. D. Foden, J. R. Prescott, H. H. Veeh, and A. W. Webb. "Geochronology in South Australia." Australian Journal of Earth Sciences 55, no. 6-7 (August 2008): 745–51. http://dx.doi.org/10.1080/08120090802094101.

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21

De Laeter, J. R. "Geochronology in Western Australia." Australian Journal of Earth Sciences 55, no. 6-7 (August 2008): 769–75. http://dx.doi.org/10.1080/08120090802094127.

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22

Nemchin, A. A., M. S. A. Horstwood, and M. J. Whitehouse. "High-Spatial-Resolution Geochronology." Elements 9, no. 1 (February 1, 2013): 31–37. http://dx.doi.org/10.2113/gselements.9.1.31.

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23

Lee, James K. W. "Multipath diffusion in geochronology." Contributions to Mineralogy and Petrology 120, no. 1 (May 1, 1995): 60–82. http://dx.doi.org/10.1007/s004100050058.

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24

de Laeter, John R. "Mass spectrometry and geochronology." Mass Spectrometry Reviews 17, no. 2 (1998): 97–125. http://dx.doi.org/10.1002/(sici)1098-2787(1998)17:2<97::aid-mas2>3.0.co;2-j.

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25

Lawley, C. J. M., and D. Selby. "Re-Os GEOCHRONOLOGY OF QUARTZ-ENCLOSED ULTRAFINE MOLYBDENITE: IMPLICATIONS FOR ORE GEOCHRONOLOGY." Economic Geology 107, no. 7 (October 12, 2012): 1499–505. http://dx.doi.org/10.2113/econgeo.107.7.1499.

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26

Gulbranson, Erik L., E. Troy Rasbury, Greg A. Ludvigson, Andreas Möller, Gregory A. Henkes, Marina B. Suarez, Paul Northrup, et al. "U–Pb Geochronology and Stable Isotope Geochemistry of Terrestrial Carbonates, Lower Cretaceous Cedar Mountain Formation, Utah: Implications for Synchronicity of Terrestrial and Marine Carbon Isotope Excursions." Geosciences 12, no. 9 (September 17, 2022): 346. http://dx.doi.org/10.3390/geosciences12090346.

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The terrestrial Lower Cretaceous Cedar Mountain Formation, Utah, is a critical archive of paleoclimate, tectonics, and vertebrate ecology and evolution. Early Cretaceous carbon cycle perturbations associated with ocean anoxia have been interpreted from this succession, as expressed in stable carbon isotopes. However, refining the timing of the observed stable isotope excursions remains a key challenge in understanding how marine anoxia affects the Earth system, and is ultimately recorded in the terrestrial realm. The geochronology and geochemistry of a terrestrial carbonate near the base of this succession, which potentially records the Ap7 global carbon isotope excursion, is studied here. Petrographic and geochemical analyses are used to test plausible mechanisms for U incorporation into the calcite lattice in this sample. Using these methods, the hypothesis that the incorporation of U was at or close to the timing of carbonate precipitation is evaluated. U–Pb geochronology of calcite indicates a plausible Early Cretaceous age. However, comparison of the new U–Pb ages of calcite with detrital zircon maximum depositional ages immediately beneath the studied sample indicates a disparity in the apparent sedimentation rates if both types of geochronologic information are interpreted as reflecting the timing of sediment deposition. The totality of data supports an early, and high-temperature, diagenetic timing of U incorporation, with potential for minor leaching of U in subsequent fluid–rock interaction. The most likely mechanism for U transport and immobilization in these samples is hydrothermal fluid–rock interaction. Therefore, the radiometric ages, and corresponding stable isotope composition of U-bearing carbonate domains in this sample, indicate early subsurface fluid–rock interactions and not a record of atmosphere–soil geochemical reactions.

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27

Kučera, Jan, Jan Kameník, Roman Garba, and Pavel P. Povinec. "Methodology and Applications of the Determination of Cosmogenic Radionuclides ¹⁰Be and ²⁶Al by Accelerator Mass Spectrometry." Chemické listy 117, no. 2 (February 15, 2023): 107–13. http://dx.doi.org/10.54779/chl20230107.

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The measurement of cosmogenic radionuclides 10Be and 26Al by accelerator mass spectrometry (AMS) has become an invaluable tool for dating events and processes in Quaternary geochronology, and in archaeology and paleoanthropology. Here we present an overview of the current state of research by providing the theoretical and methodological background and describe processes of sample preparation and measurement by AMS. We also summarize the main geochronology calculation models for exposure and burial dating for the above applications and analysis of extra-terrestrial materials.

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28

Griffin, Brendan J., Duncan Forbes, and Neal J. McNaughton. "An Evaluation of Dating of Diagenetic Xenotime by Electron Microprobe." Microscopy and Microanalysis 6, S2 (August 2000): 408–9. http://dx.doi.org/10.1017/s143192760003453x.

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Xenotime is an igneous mineral commonly present in pegmatite and fractionated granite. Recent studies reveal that it also forms as a diagenetic mineral. Minute (0.1-5 μm) xenotime overgrowths typically crystallise on the surfaces of detrital zircon shortly after sedimentation, in a wide range of siliciclastic sedimentary units. For example, in backscattered electron (BSE) imaging using a scanning electron microscope (SEM), two minute, euhedral, pyramidal, xenotime overgrowths on an oscillatory-zoned detrital Ambergate zircon are evident (figure 1).Electron microprobe analysis (EMPA) geochronology is a chemical dating method that uses precisely measured concentrations of U, Th, and Pb, and the decay rates of U238, U235, and Th232, to calculate an age for a mineral. The EMPA dating method used in this study to date igneous xenotime and igneous-metamorphic monazite is the chemical isochron method (CHIME). EMPA geochronology is not a widely used technique because of the higher precision of isotopic geochronology.

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29

Hollis, Julie A., Dirk Frei, Jeroen A. M. Van Gool, Adam A. Garde, and Mac Persson. "Using zircon geochronology to resolve the Archaean geology of southern West Greenland." Geological Survey of Denmark and Greenland (GEUS) Bulletin 10 (November 29, 2006): 49–52. http://dx.doi.org/10.34194/geusb.v10.4908.

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Until recently, in situ U-Pb zircon geochronology could be carried out only using ion microprobes, requiring lengthy analysis times of c. 20 minutes. However, new developments in laser ablation inductively coupled plasma mass spectrometer technologies have resulted in zircon geochronology techniques that are much faster, simpler, cheaper, and more precise than before (e.g. Frei et al. 2006, this volume). Analyses approaching the precision obtained via ion microprobe can now be undertaken in 2–4 minutes using instruments such as the 213 nm laser ablation (LA) system coupled with Element2 sector-field inductively coupled plasma mass spectrometer (SF-ICP-MS) housed at the Geological Survey of Denmark and Greenland (GEUS). The up to tenfold decrease in analytical time means that zircon geochronology can now be used in a much wider range of studies. The Godthåbsfjord region, southern West Greenland, contains some of the oldest rocks exposed on the Earth’s surface reflecting a very complex Archaean geological evolution (Figs 1, 2). Over recent years GEUS has undertaken a range of mapping projects at various scales within the Godthåbsfjord region (see also below). These include the mapping of the 1:100 000 scale Kapisillit geological map sheet (Fig. 1), and regional and local investigations of the environments of formation and geological evolution of supracrustal belts, hosting potentially economic mineral occurrences. Zircon geochronology is an important tool for investigating a range of geological problems in this region. By breaking down the complex geology into a series of simple problems that can be addressed using this tool, the geological evolution can be unlocked in a stepwise manner. Three examples are presented below: (1) the mapping of regional structures; (2) characterising and correlating supracrustal belts; and (3) dating metamorphism and mineralisation. Although focus is on the application of zircon geochronology to these problems, it is important to note that the resulting data must always be viewed within a wider context incorporating geological mapping and structural, geochemical and petrographic investigations.

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30

Wu, Meng, Liang Li, Jing-gui Sun, and Rui Yang. "Geology, geochemistry, and geochronology of the Laozuoshan gold deposit, Heilongjiang Province, Northeast China: implications for multiple gold mineralization events and geodynamic setting." Canadian Journal of Earth Sciences 55, no. 6 (June 2018): 604–19. http://dx.doi.org/10.1139/cjes-2018-0038.

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The Laozuoshan gold deposit, located in the central part of the Jiamusi Massif, is hosted by the contact zone between granitic complex and Proterzoic strata. In this study, we present the results of geochronology and geochemistry of ore-related granodiorite and diorite porphyry, and hydrothermal sericite 40Ar/39Ar dating. The granodiorite and diorite porphyry in the Laozuoshan gold deposit are calc-alkaline and high-K (calc-alkaline) series, which are enriched in LREE and LILE and depleted in HFSE, with no depletion of Eu. The geochronology data show that zircon U–Pb ages of the granodiorite and diorite porphyry are ∼262 Ma and ∼105 Ma, respectively. The sericite 40Ar/39Ar ages are ∼194 Ma and ∼108 Ma. On the basis of previous researches, ore geology and geochronology studies show that the Laozuoshan gold deposit underwent at least two gold mineralization events. We suggest that the first one, which was related to skarnization, resulted from the collision between the Jiamusi and Songnen Massifs in Late Permian. The subsequent gold mineralization resulted from the subduction of the paleo-Pacific Plate in Early Cretaceous.

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31

Davis, D. W. "Historical Development of Zircon Geochronology." Reviews in Mineralogy and Geochemistry 53, no. 1 (January 1, 2003): 145–81. http://dx.doi.org/10.2113/0530145.

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32

Zack, Thomas, and Ellen Kooijman. "Petrology and Geochronology of Rutile." Reviews in Mineralogy and Geochemistry 83, no. 1 (February 1, 2017): 443–67. http://dx.doi.org/10.2138/rmg.2017.83.14.

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33

Snelling, N. J. "Geochronology and the geological record." Geological Society, London, Memoirs 10, no. 1 (1985): 3–9. http://dx.doi.org/10.1144/gsl.mem.1985.010.01.02.

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34

Chamberlain, Elizabeth L. "A bright approach to geochronology." Physics Today 71, no. 9 (September 2018): 74–75. http://dx.doi.org/10.1063/pt.3.4030.

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35

Aubry, M. P., W. A. Berggren, D. V. Kent, J. J. Flynn, K. D. Klitgord, J. D. Obradovich, and D. R. Prothero. "Paleogene geochronology: An integrated approach." Paleoceanography 3, no. 6 (December 1988): 707–42. http://dx.doi.org/10.1029/pa003i006p00707.

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36

Zeitler, Peter K. "The geochronology of metamorphic processes." Geological Society, London, Special Publications 43, no. 1 (1989): 131–47. http://dx.doi.org/10.1144/gsl.sp.1989.043.01.08.

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Ovchinnikov, L. N., S. N. Voronovskiy, and L. V. Ovchinnikova. "ISOTOPE GEOCHRONOLOGY OF METAMORPHIC PROCESSES." International Geology Review 28, no. 5 (May 1986): 584–96. http://dx.doi.org/10.1080/00206818609466298.

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Penkman, Kirsty, and Darrell Kaufman. "Amino acid geochronology: Recent perspectives." Quaternary Geochronology 16 (April 2013): 1–2. http://dx.doi.org/10.1016/j.quageo.2012.12.007.

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KENT, DENNIS V., and FELIX M. GRADSTEIN. "A Cretaceous and Jurassic geochronology." Geological Society of America Bulletin 96, no. 11 (1985): 1419. http://dx.doi.org/10.1130/0016-7606(1985)96<1419:acajg>2.0.co;2.

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Vermeesch, Pieter. "Dissimilarity measures in detrital geochronology." Earth-Science Reviews 178 (March 2018): 310–21. http://dx.doi.org/10.1016/j.earscirev.2017.11.027.

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Sharman, Glenn R., and Samuel A. Johnstone. "Sediment unmixing using detrital geochronology." Earth and Planetary Science Letters 477 (November 2017): 183–94. http://dx.doi.org/10.1016/j.epsl.2017.07.044.

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Eglington, Bruce M. "DateView: a windows geochronology database." Computers & Geosciences 30, no. 8 (October 2004): 847–58. http://dx.doi.org/10.1016/j.cageo.2004.06.002.

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Brigham-Grette, Julie. "Current Trends in Quaternary Geochronology." Episodes 10, no. 1 (March 1, 1987): 43–44. http://dx.doi.org/10.18814/epiiugs/1987/v10i1/017.

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De Laeter, J. R. "Geochronology in Australia: an overview." Australian Journal of Earth Sciences 55, no. 6-7 (August 2008): 723–24. http://dx.doi.org/10.1080/08120090802094085.

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O'reilly, S. Y., W. L. Griffin, and B. Gulson. "Geochronology in New South Wales." Australian Journal of Earth Sciences 55, no. 6-7 (August 2008): 737–40. http://dx.doi.org/10.1080/08120090802094093.

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Gleadow, A. J. W., and J. F. Lovering. "Development of geochronology in Victoria." Australian Journal of Earth Sciences 55, no. 6-7 (August 2008): 753–67. http://dx.doi.org/10.1080/08120090802094119.

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Golding, S. D. "History of geochronology in Queensland." Australian Journal of Earth Sciences 55, no. 6-7 (August 2008): 741–44. http://dx.doi.org/10.1080/08120090802163567.

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Schoene, B., D. J. Condon, L. Morgan, and N. McLean. "Precision and Accuracy in Geochronology." Elements 9, no. 1 (February 1, 2013): 19–24. http://dx.doi.org/10.2113/gselements.9.1.19.

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Kohn, Matthew J. "Models of garnet differential geochronology." Geochimica et Cosmochimica Acta 73, no. 1 (January 2009): 170–82. http://dx.doi.org/10.1016/j.gca.2008.10.004.

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Aiqing, Hu, Zhu Bingquan, Mao Cunxiao, Zhu Naijuan, and Huang Rongsheng. "Geochronology of the Dahongshan Group." Chinese Journal of Geochemistry 10, no. 3 (July 1991): 195–203. http://dx.doi.org/10.1007/bf02843324.

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