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On plate tectonics and ocean temperatures
Origin and 87 Rb– 87 Sr age of porewaters in low permeability Ordovician sediments on the eastern flank of the Michigan Basin, Tiverton, Ontario, Canada
The SPICE carbon isotope excursion in Siberia: a combined study of the upper Middle Cambrian–lowermost Ordovician Kulyumbe River section, northwestern Siberian Platform
Paleobathymetry of a Silurian shelf based on brachiopod assemblages: an oxygen isotope test
Hydrothermal Effects on Isotope and Trace Element Records in Modern Reef Corals: A Study of Porites lobata from Tutum Bay, Ambitle Island, Papua New Guinea
Silurian strontium isotope stratigraphy
Cathodoluminescence investigations and trace-element analysis of quartz by micro-PIXE; implications for diagenetic and provenance studies in sandstone
Significance of aragonite cements around Cretaceous marine methane seeps
Cathodoluminescene at low Fe and Mn concentrations; a SIMS study of zones in natural calcites
Seawater strontium isotopic perturbation at the Permian-Triassic boundary, West Spitsbergen, and its implications for the interpretation of strontium isotopic data
Diagenetic stabilization of aragonite and low-Mg calcite; II, Stable isotopes in rudists
Deposition and Chemical Diagenesis of Tertiary Carbonates, Kirkuk Oil Field, Iraq
Diagenetic stabilization of aragonite and low-Mg calcite; I, Trace elements in rudists
Front Matter
Abstract This course and the accompanying text should be of value to SEPM members as well as to other geologic professionals. Stable isotope geochemistry has come into its own in the last few years as our inventory of processes and materials has improved from the result of much basic research. Stable isotope techniques should become a standard application to most studies of sedimentary rocks and depositional environments, and we emphasize that it has applications in explorat: ion for hydrocarbons and minerals as well as in basic research. However, rapid progress depends on adequate and proper education of professionals in the techniques, the correct selection of samples, consideration of problems of interpretation, and concern for other types of data required to constrain interpretation of stable isotopic data. This text is designed to supplement the Society of Economic Paleontologists and Mineralogists continuing education course dealing with the application of stable isotopes to geologic problems. Stable isotope geochemistry is taught in relatively few universities or colleges, and although a few textbooks and other volumes present general principles of stable isotope geochemistry, they contain few adequate, well documented case studies or applications to relevant problems of interest to sedimentary geologists or paleoecologists. These short notes are an integral part of this course and should also fill a void in the literature. However, we do not pretend that the coverage of topics is entirely comprehensive. For example, the reader will find relatively little concerning the stable isotopic compositions of clay minerals, biogenic silica or chert.
Stable Isotopes of Oxygen and Carbon and their Application to Sedimentologic and Paleoenvironmental Problems
Abstract Isotopes are atoms whose nuclei contain the same number of protons but a different number of neutrons. There are about 300 stable (non-radioactive) isotopes in nature. (The number of unstable, radioactive isotopes is in excess of 1200.) 62 of the 83 stable elements (H to Bi) have at least two isotopes; in most cases one isotope is predominant, the others being present in only trace amounts. To a first approximation, the isotopes of an element behave almost identically, since chemical behavior is governed by the electron structure of the atom and hence on the number of protons in the nucleus. Although this approximation is satisfactory for many experimental systems in the laboratory, it does not apply to many chemical, physical, and biological processes in nature. Differences in isotopic mass lead to subtle but significant differences in the behavior of the isotopes of an element during natural processes. This is the basis for the field of stable isotope geochemistry. The application of stable isotope variations to geological problems has focused on the elements of low atomic weight: hydrogen, carbon, nitrogen, oxygen, and sulfur. Since the magnitude of ”isotope effects“ is proportional to the relative mass difference between isotopes (Am/m), significant isotopic variations in nature are limited to the light elements. In addition, H, C, N, 0, and S occur in relatively high abundance, participate in most important geochemical reactions, and are the most important elements in biological systems. Table 1-1 lists the average abundance of the isotopes of these elements as
Stable Isotopes of Sulfur, Nitrogen and Deuterium in Recent Marine Environments
Abstract The elements to be discussed below are all biologically important and play a vital role in the metabolism and cellular synthesis by all organisms. The products of biosynthesis are deposited in the sediments and can be recognized in shales after having undergone diagenesis. Each of these elements has a distinct distribution pattern in the ocean and their isotopes are incorporated into organic matter according to controls that are largely directed by kinetic processes, involving the action of enzymes as transporting agents and cell walls as diffusion boundries. The end products of biological and diagenetic processes results in the formation of kerogen, which concentrates in the shale, or hydrocarbons which may escape and be transported out of the shale. Both early diagenetic and later maturation processes each impose changes in the isotope composition of the original starting organic matter. The average ratio of in terrestrial water is 22.6. Sulfur is an important element in the marine environment because it undergoes both organic and inorganic reactions which lead to formation of sedimentary materials. It is now well established that biological systems are capable of selectively metabolizing the stable isotopes of sulfur (Thode 1951; Jones and Starkey, 1957; Harrison and Thode 1958; Kaplan and Rittenberg, 1964) . The process can be divided into assimilatory or dissimilatory, and reductive or oxidative functions. The maximum fractionation for various metabolic processes measured by Kaplan and Rittenberg (1962) can be seen in Table 2-l. The data in this table can be dompared with the pathways
Chemical Diagenesis of Carbonates: Theory and Application of Trace Element Technique
Abstract Diagenetic histories of carbonate rocks are being deciphered mostly with the aid of textural criteria (e.g. Bathurst, 1975). Chemical critena are usually considered to be supplementary parameters only. The major stumbling block for wider utilization of chemical criteria is the lack of familiarity with these techniques as well as the absence of generalized theory which could be applied to quantification of chemical processes leading to diagenetic stabilization of carbonate sediments. The fundamental principles and applications of stable isotopes have been discussed in the previous chapters in this text. These exaniples demonstrated the advantages as well as limitations of the approach. The conclusions based on stable isotopes are, as for any other tool, frequently not unique. In such a case, it is to our advantage to possess such a complementary tool capable of focusing the choice of available options. Such a complementary tool is the trace element technique. A carbonate mineral, whether calcite, aragonite or dolomite contains, in addition to and, a plethora of trace elements (Sr. Ba, Mg, Mn, Fe, Zn, etc.) and radiogenic isotopes. In this contribution, I shall try to outline the underlying theoretical principles and the examples of application of trace elements to diagenetic studies. The contribution is not intended to be a review of all previous work related to the subject, but rather to represent a documentation of a specific approach, namely that developed by the author and associates for solution of problems tractable for this technique. Calcium carbonate minerals, fossils and sediments
The Application of Stable Isotopes to Studies of the Origin of Dolomite and to Problems of Diagenesis of Clastic Sediments
Abstract Two problems complicate the rigorous use of isotopic data to delineate the origin and diagenesis of dolomitized limestones. First, the re-lationship between δ , δodolomite . and temperature is imperfectly known, and may, in fact, depend in part on the crystal structure (composition and degree of order) of a particular dolomite under consideration. And second, the initial dolomitization of a sediment or limestone appears to be nearly open system because of the large volume of water necessary to import sufficient magnesium to cause massive dolomitization (at least 800 pore volumes of seawater, for example). But many dolomitized rocks, particularly older ones, have undergone one or more recry-stallizations to more stable dolomite phases, and these replacement reactions are certainly not open-system. The problem of interpreting recrystallization(s) in partly closed systems is not yet solved. The relationship between the isotopic composition of dolomite, temperature and the isotopic composition of water has been determined experimentally by a variety of investigators using a variety of techniques Using standard notation, All equations have been corrected to be consistent with Friedman 18 and O'Neil (1977). These relations are plotted for δwater =0 ‰ in Figure4–1. Given a dolomite analysis, and assuming open system reaction, the range in uncertainty in temperature (given or assuming a is about and the range in uncertainty in water (given or assuming a temperature) is about 4 o/oo. The difference (ti) between a co-existing calcite and dolomite ranges from about 3 o/oo to 6 o/oo at Using natural examples, mostly from