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• Front Matter
  • Contents
  • Preface
  • Acknowledgements
    • Figure acknowledgements
• 1 Introduction
  • Figure 1.1 (a) Geologists collecting data for a graphic log (Section 6.3) to record how a sedimentary succession has changed through time and to decipher the overall depositional environment. By working together they can share tasks and discuss their observations. (b) The recessed bed marks the Cretaceous–Paleogene boundary at Woodside Creek, near Kekerengu, New Zealand. Note the holes where samples have been extracted for palaeomagnetism studies. In this case the number of holes is rather excessive and breaks the code of good practice (Section 2.12 and Chapter 13). (a and b: Angela L. Coe, The Open University, UK.)
  • 1.1 A selection of general books and reference material on geology
  • 1.2 Books on geological field techniques
• 2 Field equipment and safety
  • 2.1 Introduction
    • Table 2.1 Equipment required for most geological fieldwork. Clothing and safety equipment is discussed in Section 2.11.
    • Table 2.2 Typical sampling equipment. See also Chapter 13.
    • Table 2.3 Optional and specialist field equipment.
    • Quantification of geological observations
  • 2.2 The hand lens and binoculars
    • Figure 2.1 A variety of different hand lenses. (1) Standard 10× single lens; (2) 10× lens with built-in light – the lens casing matches the focal length; (3) 8× lens with built-in light; (4) 10× and 15× dual lens.
    • Figure 2.2 Photograph to show correct use of the hand lens. Note that the person is holding the lens close to his eye. The lens is fastened on a lanyard around his neck for ease of access and use.
  • 2.3 The compass-clinometer
    • Figure 2.3 Labelled photographs of the parts of two of the most commonly used types of compass-clinometer. These terms are referred to in the text and in other figures. (a)–(c) The Brunton-type compass-clinometer: in this case the Brunton Geo. Views: (a) side; (b) top; (c) bottom. (d)–(e) Silva-type compass-clinometer: in this case the Silva Expedition 15TDCL. Views: (d) top; (e) bottom. There are small variations from model to model, with more features on some models. Compass-clinometers from other manufacturers have similar features.
    • Magnetic declination
      • Figure 2.4 (a) Simplified sketch of the Earth to show the relationship between magnetic declination, magnetic north, true north and, via the inset, the longitude, latitude and a grid system (in this case the UK grid squares). (b and c) Typical map information showing magnetic north, true north and grid north. The adjustment of the magnetic declination is shown by the red arrows; (b) is for a westerly declination of magnetic north from true north and (c) is for an easterly declination.
    • 2.3.1 Orientation of a dipping plane
      • Figure 2.5 Sketch to show strike, dip magnitude and dip direction of a plane. See also Figures 2.6 and 2.7. Using the north arrow shown this imaginary plane is striking east–west (270° or 090°) and dipping to the north. Any direction down the dipping plane that is not at right angles to the strike will be an apparent dip direction and will have a smaller dip magnitude than the true dip magnitude.
      • Determination of the orientation of a dipping plane by the contact method
        • Figure 2.6 How to use the Silva-type compass-clinometer to measure the orientation and dip of a plane using the contact method. The parts of the compass-clinometer are shown in Figure 2.3d and e.
        • Figure 2.7 How to use the Brunton-type compass-clinometer to measure the orientation and dip of a plane using the contact method. The parts of the compass-clinometer are shown in Figure 2.3 a–c.
      • Determination of the orientation of a dipping plane using the clinometer hinge of the Brunton-type compass-clinometer
        • Figure 2.8 Measurement of the dip direction and dip magnitude of a plane with the Brunton Geo compass-clinometer in one position. (a) Side view of the compass-clinometer in position for measuring both the dip magnitude and dip azimuth. (b) Close up view of the hinge area. The dip magnitude is read off where the top of cut-out intersects with the scale; in this case it is 12°. Note also the extra spirit level on the side indicating that the compass window is horizontal. (c) View of the compass window showing that the compass window is level (round spirit level) and that the dip azimuth is 098°. This bedding plane is thus orientated at 008/12E.
    • 2.3.2 Orientation of a linear feature
      • Figure 2.9 Steps in the measurement of the azimuth and plunge of a linear feature (lineament) by the contact method – for both types of compass-clinometer. The parts of the compass-clinometers are shown in Figure 2.3.
      • Contact method for measuring the orientation of a linear feature
      • Sighting method for measuring the orientation of a linear feature
        • Figure 2.10 Measurement of the azimuth and plunge of a linear feature (slickenside lineations (Section 8.2.2)) on a fault plane using the sighting method with the Brunton-type compass-clinometer. Insets show detail of line of sight. The parts of the compass-clinometer are shown in Figure 2.3 a–c.
    • 2.3.3 Triangulation: Determining location using a compass
      • Figure 2.11 Triangulation using a Brunton-type compass. The terms for the different parts of the compass-clinometer are given in Figure 2.3a–c. (Map: Ordnance Survey, Landranger Series, Sheet 81. Ordnance Survey on behalf of HMSO © Crown Copyright 2010. All rights reserved. Ordnance Survey Licence number 100018362. (extract is from within 10 km grid square NU(46)00.)
      • Figure 2.12 Triangulation using a Silva-type compass. Inset shows line of sight. The terms for the different parts of the compass-clinometer are given in Figure 2.3d and e. (Map extract as Figure 2.11. © Crown Copyright 2010. All rights reserved. Ordnance Survey Licence number 100018362.)
  • 2.4 Global positioning systems and altimeters
  • 2.5 Measuring distance and thickness
    • Figure 2.13 (a) A variety of useful tape measures for field use: 1, surveyor’s tape; 2, folding rule; 3, 1 m folding rule; 4, retracting metal-tape measure. (b) Home-made wooden pole with decimetre graduations to give a general idea of scale.
    • 2.5.1 Standard thickness and distance measurements
      • Figure 2.14 Sketch to show the basic trigonometry for obtaining a true thickness by measuring the horizontal distance between dipping beds.
    • 2.5.2 Use of the Jacob staff to measure the thickness of inclined strata
      • Figure 2.15 Sketch to show how to measure thickness up a slope with a Jacob staff of 1.5 m length and a Brunton-type compass-clinometer.
  • 2.6 Classification and colour charts
    • Figure 2.16 Use of a grain-size chart to determine the average grain size. (a) In this case the average grain size is 500 μm. The grain size varies between 375 and 750 μm. (b) Close up view of (a).
    • Figure 2.17 Highly simplified three-dimensional representation of Munsell colours. (a) The axes for value, hue and chroma within a sphere. The 10 hues are shown but for simplicity the 10 subdivisions within each hue are not shown and neither is the chroma. (b) Sphere of colour with the colours becoming lighter towards the top (increase in value). (c) Part of one segment showing very generally the increase in value towards the top and the increase in chroma towards the outer edge of the segment. (d) Part of a Munsell colour chart specially designed for rocks. In this case the grey organic-rich mudstone sample on the left has a Munsell colour of 5Y 2/1 (olive black).
  • 2.7 Hammer, chisels and other hardware
    • Figure 2.18 Some of the different geological hammers and cold chisels available on the market. (1) Estwing pick end hammer, (2) Estwing chisel end hammer, (3) cold chisel with hand guard, (4 and 5) 2.5 lb and 1 lb geological hammers with fibreglass shafts, (6) pencil chisel, (7) tile scribe and (8) 3 lb lump hammer.
    • Figure 2.19 (a) Poorly consolidated sandstone showing current-formed climbing ripples. This structure has been revealed by carefully scraping the surface of the sandstone with the edge of a trowel. An unprepared surface lies to the right and at the level of the trowel. Shellingford cross-roads quarry, Oxfordshire, UK. (Angela L. Coe, The Open University, UK.) (b) Lower Jurassic mudstones shown with the surface iron coating (yellow) and after a clean surface was obtained through vigorous wire brushing. Note how the scraped surface shows laminations that were not previously apparent. Deep scratch marks are 5 cm apart. Such slight surface abrasions quickly weather and do not pose significant conservation issues. (Anthony S. Cohen, The Open University, UK.)
  • 2.8 The hardcopy field notebook
  • 2.9 The laptop, netbook or PDA as a notebook
  • 2.10 Writing equipment, maps and relevant literature
    • 2.10.1 Writing equipment
    • 2.10.2 Maps and relevant literature
  • 2.11 Comfort, field safety and field safety equipment
    • 2.11.1 Clothes, backpack/rucksack and personal provisions
    • 2.11.2 Field safety
      • (1) Be prepared
      • (2) Assess and monitor the potential hazards
      • (3) Know what to do in an emergency
        • Working alone
    • 2.11.3 Field safety equipment
      • Figure 2.20 Geological hammer with head showing spalling (head is 12 cm long). Further use is likely to result in small sharp pieces of metal flying loose.
  • 2.12 Conservation, respect and obtaining permission
    • Table 2.4 Summary of the main code of ethics for countryside and wilderness areas.
  • 2.13 Further reading
• 3 Introduction to field observations at different scales
  • 3.1 Introduction: What, where and how?
    • 3.1.1 Defining the fieldwork objectives
      • Table 3.1 Common objectives for completing geological fieldwork and cross references.
    • 3.1.2 Deciding where to do the fieldwork
      • Table 3.2 Possible places to search for exposures. In the case of animal burrows and where trees have been disturbed the subsoil type and small pieces of rock may give an indication of the underlying unit. This type of information should be directly compared with similar data collected from where the rocks are exposed.
    • 3.1.3 Locating your position
      • Other methods of determining your position
  • 3.2 Scale of observation, where to start and basic measurements
    • 3.2.1 Regional context
    • 3.2.2 Whole exposure
      • Figure 3.1 Four photographs and accompanying line drawings of different exposures showing how they might be divided into major units for recording and further examination. (a) Jurassic strata faulted against Triassic strata at Blue Anchor, Somerset, UK (height of cliff c. 10 m). (b) Carboniferous strata at Bowden Dors, Northumberland, UK. (c) Eocene strata exposed in the Clarence Valley, South Island, New Zealand. (d) Cenozoic strata at Choirokitia gorge, Cyprus. (a–d: Angela L. Coe, The Open University, UK.)
    • 3.2.3 Hand specimens
      • Table 3.3 Reference guide to checklists, figures and tables elsewhere in the book and in the appendices (prefixed A) for rock description.
  • 3.3 Overview of possible data formats
• 4 The field notebook
  • 4.1 Introduction: The purpose of field notes
  • 4.2 Field notebook layout
    • 4.2.1 Preliminary pages
    • 4.2.2 Daily entries
      • Figure 4.1 Four examples from notebooks of the first page relating to a particular day’s field activities. (a) Visit to a working quarry to collect rock samples. (Notebook of Angela L. Coe, The Open University, UK.) (b) Field trip to Snowdonia, UK with introductory notes. (Notebook of Tiffany Barry, The Open University, UK.) (c) Geological mapping in Ireland. (Notebook of Kate Bradshaw, The Open University, UK.) (d) Field trip to Seaton Sluice, Tyne and Wear, UK to examine the sedimentary deposits. (Notebook of Paul Temple, Open University student.)
    • 4.2.3 General tips
      • Figure 4.2 (a) Sketch from a field notebook showing good use of space, a method of separating interpretation (shown in the cloud at the top right) from the observations. (Notebook of Brian McDonald, Open University student.) (b) Part of a graphic log showing effective use of colour to pick out samples (red) and photographs (blue). (Notebook of Angela L. Coe, The Open University, UK.)
  • 4.3 Field sketches: A picture is worth a thousand words
    • Figure 4.3 Example sketches from different authors’ notebooks showing features on a wide variety of scales. (a) Simple cross-sectional sketch showing wavy lamination in a sedimentary rock. (Notebook of Paul Temple, Open University student). (b) Zoned phenocryst showing shape of crystal zones. (Notebook of Kate Bradshaw, The Open University, UK.) (c) Labelled cross-sectional sketch of pebble bed. (d) Large-scale sketch cross-section across a hillside in Argentina. (c and d: Notebook of Angela L. Coe, The Open University, UK.) (e) Complex three-dimensional sketch of trough cross-stratification in a block of sandstone. (Notebook of Kate Bradshaw, The Open University, UK.) (f) Sophisticated sketch of the geological relationships of various rock bodies in a kimberlite complex, South Africa. (Notebook of Richard Brown, The Open University, UK.)
    • 4.3.1 General principles: Aims, space and tools
      • Figure 4.4 An annotated example of a field sketch showing some of the key features that can usefully be included in a sketch. This sketch is of Kimmeridgian rocks exposed in northeast Scotland. (Notebook of Angela L. Coe, The Open University, UK.)
    • 4.3.2 Sketches of exposures
      • Figure 4.5 Photograph of Carboniferous-age strata near Cresswell, Northumberland, UK and series of sketches showing how a field sketch of this exposure might be gradually constructed. Note that features of no interest such as the large cracks have been ignored because they would detract from the geological features of interest. The rock face is depicted in the sketch as if it has been projected on to a two-dimensional vertical plane. (Notebook of Angela L. Coe, The Open University, UK.)
      • Figure 4.6 (a) Photograph and (b) sketch of a fold near Berwick-upon-Tweed, UK illustrating the technique of tracing several key beds through the structure in order to illustrate its overall form. (Notebook and photograph of Angela L. Coe, The Open University, UK.)
      • Figure 4.7 Detailed sketch of part of a kimberlite complex, South Africa illustrating use of an accurate horizontal scale in addition to good use of colour, clear labelling that does not interfere with the sketch and distinct boundaries between the different units. (Notebook of Richard Brown, The Open University, UK.)
    • 4.3.3 Sketching metre- and centimetre-scale features
      • Figure 4.8 (a) Photograph of several plunging folds near Berwick-upon-Tweed, Northumberland, UK. (b) Detail of (a) showing lines of cross-sections in (c). (c) Series of simple sketch cross-sections and a sketch map from a field notebook showing how the three-dimensional characteristics of these folds might easily be recorded in two dimensions. The map could be improved by adding a numerical value for the strike direction of the axial traces. (Photographs and notebook of Angela L. Coe, The Open University, UK.)
    • 4.3.4 Sketch maps
      • Figure 4.9 Examples of different types of sketch map constructed to show the position of important geological information. (a) River section in Argentina to show the location of a series of graphic logs. Note the GPS readings for key topographical features (a, b, c, etc.) and cross references to notebook pages where the graphic logging notes are located. The map would have been better with a north directional arrow rather than the E and W because these make it look like a cross-section. (b) Simplified map of a disused quarry, Oxford, UK showing the location of the two different sections that were measured (1 and 2). (c) Sketch map of Choirokoitia gorge, Cyprus showing the main topographical features and the relative position of further notes (A to F). (d) Detailed sketch map of about 400 × 400 m of the floor of a kimberlite mine, South Africa showing the relationship between the different rock types. Colour and abbreviations for the rock classification have been used very effectively to distinguish these complex relationships. (a to c: Notebook of Angela L. Coe, The Open University, UK; (d) Notebook of Richard Brown, The Open University, UK.)
      • Figure 4.10 Example of an enlarged, to scale and orientated detailed map produced in the field at a higher resolution than the field map to show the details of several thin beds. Note that the main topographical features have been included along with the orientation and scale. (Notebook of Kate Bradshaw, The Open University, UK.)
  • 4.4 Written notes: Recording data, ideas and interpretation
    • 4.4.1 Notes recording data and observations
      • Figure 4.11 Extracts from field notebooks showing examples of written data styles. In all cases the data are clearly laid out and easy to find. (a) List of the main minerals in an igneous rock and the characteristics of each of the minerals. (Notebook of Paul Temple, Open University student.) (b) Main observations at one locality in an area that was being mapped. (Notebook of Kate Bradshaw, The Open University, UK.) (c) Ordered and systematically recorded structural data of both planes and linear features with the dip recorded as a two-digit number and the strike as a three-digit number. Note: Ss = main foliation, Ls = main stretching lineation, Lf = fault lineation; the other abbreviations refer to minerals. See Section 8.1.1 for structural notation. (Notebook of Tom W. Argles, The Open University, UK.) (d) Description of a sedimentary rock based on a checklist of compositional and textural characteristics (see Appendix A6, Table A6.1). (Notebook of Brian McDonald, Open University student.)
      • Figure 4.12 Extracts from field notebooks showing examples of checklists. (a) Tasks to be completed and possible timing. (Notebook of Tiffany Barry, The Open University, UK.) (b) Simple ‘to do’ list. (Notebook of Clare Warren, The Open University, UK.) (c) Example of a rock sample list. (Notebook of Kate Bradshaw, The Open University, UK.)
    • 4.4.2 Notes recording interpretation, discussion and ideas
      • Figure 4.13 (a) Written interpretation in note form with clear indication of the source. (Notebook of Susan Ramsay, University of Glasgow, UK.) (b) Simple figure to summarize different interpretations of an observation. (Notebook of Brian McDonald, Open University student, UK.)
      • Figure 4.14 Examples of how interpretation might be recorded in the field. (a) Three cartoons to illustrate a possible interpretation of a fold with a cross-cutting breccia (Notebook of Tiffany Barry, The Open University, UK.) (b) Cartoon and notes interpreting a kimberlite deposit, South Africa. Excellent example of recording the hypothesis, evidence and questions that it raises. These type of notes will form a good aide memoire when the work has to be written up and as a basis of any further discussion (Notebook of Richard Brown, The Open University, UK.)
  • 4.5 Correlation with other data sets and interpretations
• 5 Recording palaeontological information
  • 5.1 Introduction: Fossils are smart particles
    • 5.1.1 Why are fossils important?
    • 5.1.2 Collecting fossil data
  • 5.2 Fossil types and preservation
    • 5.2.1 Body fossil classification
      • Figure 5.1 Part of a field notebook page showing sketches of leaves. Note scale, careful attention to venation and references to accompanying photographs, sedimentary units and specimen numbers. (Notebook of Robert A. Spicer, The Open University, UK.)
    • 5.2.2 Body fossil preservation
      • Worked Example 5.1 Using morphological observations to infer mode of life
        • Figure 5.2 Two echinoid specimens with distinctly different morphologies. (a) Archaeocidaris (Robert A. Spicer, The Open University, UK) and (b) Micraster (specimen from Peter R. Sheldon, The Open University, UK).
    • 5.2.3 Trace fossils
      • Figure 5.3 Modes of fossil preservation: (a) Mummified body of a young mammoth found in Siberia; (b) polished transverse section of a permineralized (petrified) tree fern stem; (c) cast of a tree fern trunk; (d) leaf impression from the north slope Alaska. (a–d: Robert A. Spicer, The Open University, UK.)
      • Figure 5.4 Sketches to show a variety of spreiten patterns in the trace fossil Diplocraterion formed in response to deposition and erosion. (a) Stable situation where no sediment deposition or erosion is taking place. In (b) sediment has been deposited causing the organism to migrate upwards leaving traces of the original burrow as disturbed sediment below. In (c) erosion has caused the organism to burrow deeper leaving disturbed sediment (spreiten) between the vertical burrows. Figures 6.3e and 6.3f (p. 113) show fossilized Diplocraterion.
    • 5.2.4 Molecular fossils
  • 5.3 Fossil distribution and where to find them
    • 5.3.1 Transported or life position?
      • Figure 5.5 Trees stranded in a shallow river in Alaska showing similar orientation. River flow is from right to left. Trees are about 10m long. (Robert A. Spicer, The Open University, UK.)
      • Figure 5.6 Infaunal bivalve in life position from the Jurassic, near Scarborough, UK. (Angela L. Coe, The Open University, UK.)
      • Figure 5.7 Sketch to show single valves oriented (a) concave up as a result of settling from suspension and (b) convex up as a result of lateral current flow.
  • 5.4 Sampling strategies
    • 5.4.1 Sampling for biostratigraphic or evolutionary studies
      • Figure 5.8 Three different patterns of continuous or channel sampling. (a) Overlapping samples parallel to bedding. (b) Repeat samples at right angles to bedding within a lithology. (c) Samples at right angles to bedding representing the stratigraphy, with short overlaps for cross-correlation purposes.
      • Figure 5.9 Example of a trench through diatomite in China. Successive samples were obtained as the trench was dug. (Robert A. Spicer, The Open University, UK.)
      • Figure 5.10 Example of a field notebook page showing the position of fossiliferous layers and pollen samples on a graphic log. The log and samples are for a section in Assam, India. (Notebook of Robert A. Spicer, The Open University, UK.)
    • 5.4.2 Sampling of bedding surfaces and palaeoecology
      • Three-dimensional sampling
        • Figure 5.11 Cutting volumes of clays containing fossils using a carbide-tipped chainsaw. The advantage of this technique is that the samples can be taken back to the laboratory for detailed analysis. (Robert A. Spicer, The Open University, UK.)
      • Determining quadrat size – rarifaction or species/area (or volume) curves
        • Figure 5.12 (a) The dependence of abundance estimates and, in particular, percentage frequency on the size of quadrat used in relation to the plant fragment size. If a quadrat of the size shown (small red square) were used to sample this bedding surface there would be a marked discrepancy in estimated abundance for the two taxa, irrespective of their actual relative abundance, because the quadrat size is similar to that of one of the taxa. (b) A rarefaction curve showing increasing numbers of taxa with successive doublings of quadrat size. As the quadrat size is increased more taxa occur within the quadrat, but above the point where the curve flattens out larger quadrat sizes become an inefficient way of sampling. The dashed line indicates the minimum quadrat size for this population, in which something in the order of 34 taxa might be expected to occur within each quadrat. (c) Quadrat size in relation to distribution pattern. A–C represent three forms of pattern that a taxon might exhibit: A, regular; B and C, clumped distributions of different sizes and distribution. In each area the number of specimens is the same but if a quadrat of the size shown were used for sampling very different estimates of abundance would be obtained. (d) Detection of contagions (clumping) within an assemblage. If the quadrat size is increased and the mean square (variance) is plotted, the peaks reveal the scales of clumping.
      • Pattern
      • Edge effects
  • 5.5 Estimating abundance
    • 5.5.1 Presence/absence and qualitative abundance estimates
      • Table 5.1 Typical simple subjective abundance classes and their numerical equivalents.
    • 5.5.2 Quantitative measures of abundance
      • Frequency
      • Density
      • Cover
        • Worked Example 5.2 Measuring abundance
          • Figure 5.13 Correspondence analysis of samples from the Jurassic plant fossil locality at Hasty Bank, Yorkshire, UK. The diagrams show three faces of a hollow cube onto which the positions of samples are projected from three-dimensional space; this means that each plot has three times as many points as there are samples. The three sides of the cube represent the first three axes of greatest variation in the analysis. The sample points are numbered for cross referencing. Samples from siltstones are represented as open blue circles while closed red circles represent samples from claystones. (a) Abundance counts. (b) The same data but with abundance transformed into a logarithmic simple abundance class measure similar to that shown in Table 5.1. In plot (b) much of the ‘noise’ in the data has been removed and the pattern of plant associations in the two different sedimentary facies is more clearly displayed. (Modified from Spicer and Hill 1979.)
        • Figure 5.14 (a) Line drawing of Jurassic plant fossils from Cayton Bay, Yorkshire, UK, made from an exposed bedding plane with an overlain 0.5m × 0.5m point quadrat shown in (b). For purposes of visualization the 100 randomly distributed points have been expanded into yellow circles.
      • Percentage scores and other ‘closed’ measures
      • Logarithmic transforms and the reduction of ‘noise’
    • 5.5.3 How many samples are required?
      • Figure 5.15 As the number of samples taken rises so the fluctuation in the value of the cumulative mean of the number of taxa will decrease. The point at which the variation stabilizes (in this case between 25 and 30) indicates the minimum number of samples required to investigate that population.
  • 5.6 Summary
  • 5.7 Further reading
• 6 Recording features of sedimentary rocks and constructing graphic logs
  • 6.1 Introduction
    • Figure 6.1 An example of a small part of a section of sedimentary strata from which a lot of information about the depositional processes can be gained. The image shows cross-stratification produced by the migration of wave-formed ripples indicating that the sediments were deposited within wave base (less than tens of metres depth) by waves. Some of the ripples near the middle of the image are climbing, indicating high sedimentation rates. The image shows colour variation that is likely to reflect grain and/or compositional changes, which may relate to changing energy or sediment source. There are also several trace fossils indicating animal activity. Carboniferous-age strata exposed near Berwick-upon-Tweed, UK. (Angela L. Coe, The Open University, UK.)
  • 6.2 Description, recognition and recording of sedimentary deposits and sedimentary structures
    • 6.2.1 Recording sedimentary lithology
      • Siliciclastic rocks
      • Mudrock
        • Figure 6.2 (a) Blocky fracture pattern of a siliciclastic mudrock mainly composed of clay minerals. (b) Conchoidal fracture pattern of a mudrock with a significant proportion of carbonate. (a and b: Angela L. Coe, The Open University, UK.)
      • Conglomerates and breccias
      • Carbonates
        • Table 6.1 Sedimentary rock types and the sedimentary structures and features that they are commonly associated with. Section 6.2.2 considers sedimentary structures more fully.
    • 6.2.2 Recording sedimentary structures
      • Figure 6.3 Paired photographs of sedimentary structures taken from orthogonal faces. (a) Cross-stratification. Note that from this one view it is impossible to tell whether it is trough or planar stratification. (b) This is from the same bed as (a) and shows distinct troughs indicating that (a) and (b) are part of a trough cross-stratified deposit. (c and d) Hummocky cross-stratification (HCS) showing that the structure is similar no matter which section is viewed. (e) Diplocraterion burrow showing the plan view of this vertical burrow. The circles are the top of the tubes and the lines joining them are the disrupted sediment in between. (f) Cross-section view showing the vertical U-tube and spreiten. This view is more typical of that illustrated in the literature. Figure 5.4 (p. 86) shows an idealized cross-sectional view of Diplocraterion. (a–f: Angela L. Coe, The Open University, UK.)
      • Table 6.2 Some of the common depositional sedimentary structures, bedforms (marked) and their process of formation. Note: cross-stratification refers to both cross-bedding and cross-lamination with no scale implication. Figure numbers prefixed with an A can be found in Appendix A6.
      • Table 6.3 Some of the common erosional sedimentary structures and their processes of formation. Figure numbers prefixed with an A can be found in Appendix A6.
      • Table 6.4 Some of the common early and late post-depositional sedimentary structures and their processes of formation. Figure numbers prefixed with an A can be found in Appendix A6.
  • 6.3 Graphic logs
    • Figure 6.4 A neat version of a typical graphic log with some of the key features labelled. The field version should look very similar except it might not be drawn to scale vertically and there might be other columns with samples, photographs and links to more detailed notes on particular contacts and/or units. For examples of field graphic logs see Figures 4.2b, 5.10, 6.9b, 6.11 and the book cover.
    • 6.3.1 Conventions for graphic logs
      • Figure 6.5 Variety of different grain-size scales. (a) Basic scale for siliciclastic rocks. (b) A more technically correct scale with each of the subdivisions representing a doubling in grain-size diameter for the sand subdivision (but this can be harder to distinguish in the field and does not necessarily add that much more information). (c) Grain-size scale for carbonate rocks. (d) Potential subdivisions based on composition for mudstone successions. For mixed siliciclastic carbonate rocks both grain-size scales are often added to the graphic log.
      • Variations on the conventions for graphic logs
        • Figure 6.6 Same graphic log as Figure 6.4 but with the sedimentary structures and lithology in two separate columns.
    • 6.3.2 Constructing a graphic log
      • Figure 6.7 (a) Some options for notebook layout for graphic logging. (b) Header of an example graphic logging sheet.
      • Figure 6.8 Sketch of an erosion surface in the Carboniferous, Northumberland showing the large-scale topography on the surface and details of the laterally variable units above and below. (Notebook of Angela L. Coe, The Open University, UK.)
      • Worked Example 6.1 Construction of a graphic log of a shallow-water carbonate succession
        • Figure 6.9 Field data. (a) Photographs of part of the exposure at Freshwater Bay, Isle of Portland, UK. (b) Two pages of a field notebook showing part of the graphic log constructed in the field. Note that the field log is drawn only to an approximate scale. (a and b: Angela L. Coe, The Open University, UK.)
        • Figure 6.10 The published version of the graphic log from Freshwater Bay, Dorset including the data shown in Figure 6.9. (From Coe 1996.)
  • 6.4 Rocks in space: Reconstructing sedimentary environments and their diagnostic features
    • Figure 6.11 Example of a generalized graphic log from a field notebook incorporating, in part, the beds shown in Figures 6.4 and 6.6. (Angela L. Coe, The Open University, UK.)
    • Table 6.5 Summary of some of the processes/features and the sedimentary environments that they might represent. In all cases it is the combination of different lines of evidence that will help to determine the depositional environment.
    • Worked Example 6.2 Meandering river depositional environment: Burniston, Yorkshire, UK
      • Figure 6.12 Photographs of the exposure near Burniston, Yorkshire, UK, showing the highly variable nature of the deposits. (a) General overview showing a channel sand body encased in floodplain mudstones. (b) Trough cross-stratified clean sandstones of the river channel. (c and d) Cross-cutting nature of a point bar. (e) Roots in a crevasse-splay sandstone facies. (f) Gutter casts at the base of the crevasse-splay sandstone. (g) Interbedded mudstones and sandstones interpreted as overbank deposits and crevasse splays. The dark-grey bed is a plant-rich mudstone interpreted as an ox-bow lake sediment plug. (a–g: Angela L. Coe, The Open University, UK.)
      • Figure 6.13 (a) Extract of part of an aerial photograph of the foreshore at Burniston, Yorkshire, UK and (b) part of a line drawing showing the foreshore in (a) with the distinct curved features interpreted as point bars and counter point bars. (From Alexander 1992.)
      • Figure 6.14 Three-dimensional block model and idealized cross-section to illustrate the depositional environment interpreted for the Long Nab Member, Yorkshire, UK. The right-hand part of the cross-section relates directly to the deposits at Cromer Point shown in Figure 6.11c and d. (From Alexander 1992.)
  • 6.5 Using sedimentary rocks to interpret climate change and sea-level change
    • 6.5.1 Climate change
    • 6.5.2 Sequence stratigraphy and relative sea-level change
      • Worked Example 6.3 Set of photographs and sketches to illustrate a key sedimentary contact
        • Figure 6.15 (a) Photomontage of the cliff at Bran Point, Osmington Mills to show the erosive nature of the unit near the middle of the cliff and line drawing showing the erosive surface. Inset box shows position of (b). (b) Detail of the downcutting from near the middle of the section and line drawing showing the truncation. (a and b: Angela L. Coe, The Open University, UK.)
        • Figure 6.16 Extract from a published graphic log of the most complete part of the succession across the sedimentary contact shown in Figure 6.15. (From Coe 1995.)
  • 6.6 Further reading
• 7 Recording features of igneous rocks
  • 7.1 Equipment, basic tips and safety
  • 7.2 Field relationships of igneous rocks
    • 7.2.1 Relationships with surrounding rocks
      • Figure 7.1 A dyke of Cenozoic age cutting discordantly across complexly folded wackes (Augrim quarry, Co. Down, Northern Ireland). The dyke is the 2-m-wide reddish feature, passing nearly vertically up the rock face behind the person in the foreground. (Richard Warner, British Geological Survey and Donald Fay, Open University Geological Society, UK.)
      • Figure 7.2 A complicated intrusive contact between a pale intrusive rock and a darker country rock (Oman, Arabia). In this example, the intrusive rock (here a plagiogranite or trondhjemite) has made space for itself by the process known as ‘stoping’, in which blocks of the country rock (dolerite, in this case) are plucked away and engulfed within the intrusion (where they may then become assimilated). (David A. Rothery, The Open University, UK.)
      • Table 7.1 Possible landscape clues to the location of an unexposed contact.
      • Figure 7.3 A near-vertical dyke cutting bedded sedimentary rocks (Howick Bay, Northumbria, UK). Both edges (margins) of this 1-m-wide dyke are clear. (Angela L. Coe, The Open University, UK.)
      • Figure 7.4 Schematic plan view of the possible outcrop pattern of radial dykes around a volcanic centre: (a) in the absence of regional stress and (b) with east–west extension.
      • Figure 7.5 Block-view of (a) cone sheets and (b) a ring dyke, showing their typical outcrop pattern and relationship to a magma chamber (which would solidify to form a pluton). The ground surface shown in (b) has not yet been eroded, and the circular depression bounded by the ring dyke is a volcanic caldera.
      • Figure 7.6 The base of a sill (Teesdale, Co. Durham, UK). Buff coloured fine-grained sandstones occur below the level of the person’s shoulder. The base of the sill is not actually in the obvious recess at head-height where, especially on the weathered surface, the colour changes. This is a thin siltstone layer overlain by a further c. 1 m of sandstone. Close study in the field with the aid of a hand lens reveals that the base of the sill is at the level indicated by the arrows. (David A. Rothery, The Open University, UK.)
      • Figure 7.7 (a) Sketch cross-section showing the typical relationship between a sill (in this example fed by a dyke on the left) and horizontal strata intruded by it. The sill is generally concordant, but is locally discordant where it steps up or down between strata. The lava flow is concordant. (b) As (a) but in this case the strata into which the sill and dyke were intruded have been tilted. At a later date lava flowed over the area. In this case the lava flow is discordant.
    • 7.2.2 Internal architecture: Joints and veins
      • Figure 7.8 Columnar joints developed perpendicular to the margin of a near-vertical dyke, Hvalfjorður, Iceland. (a) General view. (b) Close-up. Coin for scale. (David A. Rothery, The Open University, UK.)
      • Figure 7.9 The Fingal’s Cave flood basalt on Staffa, Inner Hebrides, Scotland. The cliff is nearly 40 m high. The base of the flow is the thin, slightly rubbly horizon at the bottom of the columns (at the roof of the cave). Columns are remarkably regular in the colonnade forming the lower 15 m of the flow, above which the joints of the entablature are more closely spaced and fan out into a variety of orientations. The original flow was probably virtually horizontal, but has been tilted by about 3° to the east (right). (David A. Rothery, The Open University, UK.)
      • Table 7.2 Distinguishing characteristics of veins in igneous rock.
      • Figure 7.10 A wave-eroded exposure cut into the colonnade of the Fingal’s Cave flow (about 200 m to the right of Figure 7.9). Note the clear shapes of the columns. (David A. Rothery, The Open University, UK.)
    • 7.2.3 Internal architecture: Other exposure-scale fabrics
      • Figure 7.11 The side of a road-cutting exposing the massive interiors and rubbly tops of ‘a’a flows in Hawaii. (David A. Rothery, The Open University, UK.)
      • Figure 7.12 Vesicles within an ’ a’ a lava flow, seen in cross-section. (a) General view, showing how vesicles become larger towards the top of the flow. (b) Close-up within the grey, central, part of the flow revealing that millimetre-and centimetre-scale vesicles are very abundant. Mount Etna, Italy. (a and b: David A. Rothery, The Open University, UK.)
      • Figure 7.13 Page from a field notebook recording observations and ideas that were later tested in the laboratory. These are good notes but there is no scale to go with the sketches. (Notebook of Janet Sumner, The Open University, UK.)
      • Figure 7.14 Unusually well-preserved and easily distinguished pillow lavas. Oman, Arabia. (David A. Rothery, The Open University, UK.)
      • Chilling and chilled margins
        • Worked Example 7.1 Impact vesiculation
        • Figure 7.15 Dyke chilled margins. (a) The chilled margin runs from top to bottom of this view parallel to the pen. Its location is indicated by the arrow drawn in the deliberately positioned field notebook. This exposure is weathered and fragmented, but there is a slight darkening on fresh surfaces from left to right towards the chilled margin. To the right of the chill, the intruded rock is the interior of another dyke. (b) Chilled margin of dyke (right) against gabbro (left). Note the inclusion of the compass in the photo, to show the strike (Oman Ophiolite, Arabia). (a and b: David A. Rothery, The Open University, UK.)
      • Pyroclastic rocks
        • Worked Example 7.2 Chilling statistics in Cyprus
          • Figure 7.16 Schematic diagram of an east–west traverse across sheeted dykes in Oman (similar to those in Figure 7.15). The tick on the chilled margins shows the direction of chilling. Numbers identify dykes, but not their order of intrusion. The east end of section A and the west end of section B are separated by a 20 m fault zone of poor and confused exposure. There is another fault zone between dykes 9 and 10. (From Lippard et al. 1986.)
        • Figure 7.17 Accretionary lapilli in this fall deposit are recognizable by their spheroidal shape and (where exposed) their concentric internal structure. (Peter Francis, The Open University, UK.)
        • Figure 7.18 Squashed pumice clasts (dark) within the paler ash matrix of the Bandelier Tuff, a 1.14 Ma ignimbrite erupted from Valles caldera, New Mexico. (Peter Francis, The Open University, UK.)
        • Figure 7.19 Cross-stratification in a pyroclastic surge deposit, including clear variations in clast size. This example is only weakly cemented, and the holes are where geologists or other animals have dug away at the rock face. Campi Flegrei, Italy. (David A. Rothery, The Open University, UK.)
        • Figure 7.20 Part of a field notebook, containing a log with preliminary interpretation of a near-vent section of the 11.4 Ma Wilson Creek Ignimbrite, Snake River Plain, Idaho, USA. The scale (given elsewhere in the notebook) is 1 m per ruled division on the page. (Notebook of Janet Sumner, The Open University, UK.)
  • 7.3 Mineralogy and small-scale textures of igneous rocks
    • 7.3.1 Petrologic type
    • 7.3.2 Mineral texture and fabric
      • ‘Flow banding’ or ‘flow foliation’
      • Cumulate layering
        • Figure 7.21 Cumulate layering in a gabbro in the Oman Ophiolite, Arabia. Dark olivine-rich layers with sharp bases gradually become more felsic upwards, repeated in a scale of a few centimetres. On this weathered surface, the felsic layers are reddened. As can be seen from the orientated compass-clinometer, in this example the layers strike approximately 060° and dip steeply northwards. (David A. Rothery, The Open University, UK.)
        • Worked Example 7.3 Dyke rooting and overlapping spreading centres in the Oman Ophiolite
      • Pegmatites
      • ‘Enclaves’
        • Figure 7.22 Autolith, 60 cm long, in the Shap Granite, Cumbria, UK. On close examination, it turns out that the autolith is not mafic (as would be implied by its colour). It is a microgranite, with a higher proportion of biotite than the coarse-grained granite that encloses it. (David A. Rothery, The Open University, UK.)
  • 7.4 Recent and active volcanoes
    • 7.4.1 Equipment and safety
      • Figure 7.23 The shelly skin of this recent pahoehoe flow gave way under the weight of this volcanologist. Wisely, he is wearing long trousers (rather than shorts) that would have protected his shins if he had stumbled into the sharp, glassy rim (Kilauea, Hawaii). A far worse accident would have been to have broken through the roof over an active lava tube. (David A. Rothery, The Open University, UK.)
      • Figure 7.24 Two infrared thermometers and one infrared video camera have been set up to look into this skylight on an inflating pahoehoe field, to record variations in the rate of flow in a lava tube on Kilauea, Hawaii. (David A. Rothery, The Open University, UK.)
    • 7.4.2 Access
    • 7.4.3 Observations
  • 7.5 Further reading
• 8 Recording structural information
  • 8.1 Equipment and measurement
    • 8.1.1 Structural measurements and notations
      • Table 8.1 Notations for structural orientation data.
  • 8.2 Brittle structures: Faults, joints and veins
    • 8.2.1 Planar brittle features – orientation
      • Figure 8.1 (a) Perspective view of a gently-dipping thrust plane (arrowed contact between dark strata in hanging wall and pale strata in the footwall) which follows topographic contours: Keystone thrust, Nevada, USA. Distance between arrows is about 20 km. (b) A major strike-slip fault (arrowed) cuts across topography in this image showing relief on the South Island of New Zealand, generated using radar from the Space Shuttle. (c) Steep faults offsetting tilted strata in this satellite image, southern Pakistan. (d) River valleys aligned along faults (dashed red lines) in this satellite image near Lake Baikal, Russia. Inset is a modified Landsat image that highlights the pronounced offset of a river (blue) across a strike-slip fault (dashed red lines). (a: Generated from U.S. Geological Survey Landsat image and National Elevation Dataset; b and c: courtesy of the U.S. Geological Survey / NASA images; d: Modified from U.S. Geological Survey / NASA MODIS and Landsat images.)
      • Table 8.2 Landscape clues to the presence of faults.
      • Figure 8.2 Landscape clues to faults. (a) Line of fault runs obliquely from left (just behind lambs) to right, marked by a break in slope and low scarp (with gorse), northeast England. (b) Hard, mineralized fault rock forms a ridge c. 10 m high along the Highland Boundary Fault, Garron Point, Scotland. (c) A sag pond in a depression along the San Andreas Fault, Carrizo Plain, California. (d) A steep normal fault (arrowed) marked by vegetation contrast cuts across topography in southern Spain. (e) Wallace Creek, a stream offset across the San Andreas Fault (arrowed), California. (a and b: Angela L. Coe, The Open University, UK. c: Courtesy of the U.S. Geological Survey. d: Tom W. Argles, The Open University, UK. e: Courtesy of the U.S. Geological Survey; photographer Bob Wallace.)
      • Figure 8.3 (a) Measuring an uneven plane with the aid of a clipboard. Remember to ensure that any metal clips are not affecting the measurement. (b) Measuring the dip of an irregular fault by sighting using the compass-clinometer. Inset shows orientation of the compass-clinometer and detail of the line of sight. (c) A set of subsidiary fractures (thin arrows) with a consistent angular relationship to the main fault zone (thick arrows). These are Riedel fractures (Section 8.2.2), evidence that the fault downthrows to the right. (a and c: Tom W. Argles, The Open University, UK. b: Angela L. Coe, The Open University, UK.)
      • Figure 8.4 (a) Conjugate veins, with a characteristic X-shaped pattern and minor offsets (Switzerland). (b) Diagram of shear and extensional fractures on a fold (based on McClay 1991); (c) Unloading joints in granite exposure near Balmoral, Scotland, UK: two sets are subvertical, almost at right angles to each other, while the third set is roughly parallel to the land surface. (d) Chaotic veins in this exposure suggest hydraulic fracturing under high fluid pressure (Wales, UK). (a, c and d: Tom W. Argles, The Open University, UK.)
      • Figure 8.5 Stylolite picked out in white limestone by red, insoluble iron oxide. Scale = 5 cm. (Tom W. Argles, The Open University, UK.)
    • 8.2.2 Determining past motion on brittle structures
      • Figure 8.6 (a) Mineral fibres in this vein grew at right angles to the vein walls, showing that it is a dilational vein. Vein is 15 mm wide at top of image. Southwest Wales, UK. (b) Slickenfibres of quartz showing oblique slip (parallel to hammer shaft) on a minor thrust fault in the Himalaya, north Pakistan. Direction of movement of the upper block is right to left, parallel to handle of hammer. (c) Steep striations (i.e. slickenside lineations) on a fault in limestone in the Swiss Alps indicate dip-slip motion. Subhorizontal ridges may record successive slip episodes, but not the sense of motion. (a–c: Tom W. Argles, The Open University, UK.)
      • Figure 8.7 (a) This outcrop pattern of simple offset strata suggests a simple sinistral strike-slip fault, as shown in (b), but the pattern could also be produced by normal (c) or reverse (d) faulting.
      • Figure 8.8 Matching corresponding piercing points, in this case where a dyke (red) intersects a lithostratigraphic boundary, is the best method for determining overall displacement on a fault. Linear features, such as a river channel in a sedimentary succession, are quite rare in the rock record. The most common type of situation is where two planar features intersect along a line, as here.
      • Figure 8.9 (a) Arrows mark individual steps and indicate slip direction of the missing block on this slickenside in southwest Wales, UK. Field of view 6 cm across. (b) Secondary fractures may develop that produce a stepped effect opposite to that in (a). (c) The pattern of en échelon vein arrays indicates relative shear sense, confirmed in this example by the deflection of dark solution seams through the shear zone that caused vein formation (southwest Wales, UK). (d) Some features within a wider shear zone that can be used to diagnose sense of shear (Riedel fractures, antithetic Riedel fractures, gouge fabrics, broken clasts). (a and c: Tom W. Argles, The Open University, UK.)
      • Figure 8.10 (a) Examples of orientated ‘thumbnail’ sketches of kinematic indicators from a field notebook. (b) An orientated sketch of structural features in a larger exposure. (Notebook of Tom W. Argles, The Open University, UK.)
      • Worked Example 8.1 Investigating a fault zone in Andalucía
        • Figure 8.11 View looking ESE along a narrow outcrop of Neogene sedimentary rocks (underlying brown field) that separates coherent schists (steep slopes to right) from fault rocks (pale knoll left of centre). Near El Chorro, southern Spain. (Tom W. Argles, The Open University, UK.)
        • Figure 8.12 Variable minor fracture plane data (blue arcs) and slickenline data (red dots) represented on a stereographic plot. The main group of fracture plane data is interpreted to approximate to the overall fault zone orientation (dipping moderately NE), while the main cluster of lineation data marks the overall slip direction (plunging gently NNW).
        • Figure 8.13 Kinematic indicators from the fault zone. (a) Broken clast of quartz vein within fault zone. (b) Suspected Riedel fractures near edge of zone. (Notebook of Tom W. Argles, The Open University, UK.)
      • Figure 8.14 Estimating throw on a fault from known stratigraphy. (a) Two units are juxtaposed across a fault in the field. (b) Possible estimates of throw compared with true throw. (c) Block diagram representing theoretical situation if no erosion had acted on the faulted landscape.
  • 8.3 Ductile structures: Shear zones, foliations and folds
    • 8.3.1 Orientation of ductile planar features
      • Figure 8.15 Examples of tectonic foliations. (a) Mylonitic foliation, northwest Himalaya. High strain is indicated by the strong planar fabric and tightly wrapped porphyroclasts with tails streaked out into the fabric. (b) Slaty cleavage, visible as fine lines running from top left to lower right (two separate cleavage planes are arrowed). The cleavage cuts obliquely across bedding (dark/pale subhorizontal layers) in these fine-grained mudstones and siltstones from Cumbria, UK. (c) Spaced fractures (arrowed) cut across subvertical bedding in a limestone, southwest Wales, UK. This fabric is sometimes referred to as ‘fracture cleavage’. (d) Pressure solution cleavage (thin, dark lines) in siltstones, west Wales, UK. Note also the cleavage refraction, where cleavage orientation changes abruptly across some bedding planes (arrowed), reflecting grain-size changes. There is also a very fine (barely visible) slaty cleavage parallel to the solution cleavage. (e) Subhorizontal crenulation cleavage in schist, NW Himalaya, showing clear microfold hinges. (f) Close-up view looking down on schistosity planes showing visible mineral grains, including mica. The surface of the sample cuts through numerous, irregular, millimetre-scale foliation planes. View is 4 cm across. (a–f: Tom W. Argles, The Open University, UK.)
      • Table 8.3 Some common tectonic fabrics.
      • Figure 8.16 High-strain features typical of mylonites. (a) Boudinage of a competent layer, northwest India. (b) Intrafolial folds, northwest India (view about 1.5 m across). (Tom W. Argles, The Open University, UK.)
      • Figure 8.17 Gneissic banding: compositional layering on a centimetre scale in a coarse-grained gneiss, Bhutan. It is difficult to tell whether this banding has a sedimentary, tectonic or metamorphic origin without detailed petrographic or geochemical analysis (Tom W. Argles, The Open University, UK.)
    • 8.3.2 Direction of shear/stretching: Stretching lineations
      • Figure 8.18 Stretching lineations. (a) Stretching lineation defined by stretched grains of quartz and biotite in a mylonitic quartzite (5 cm across). (b) Weakly aligned orthopyroxene grains roughly define the stretching direction in a mantle peridotite (base of sample is 10 cm across). (c) Stretching lineation defined by elongate amphibole crystals in an amphibolite that lacks foliation (base of sample is 8 cm across). (d) High-strain gneiss with orthogonal faces cut parallel (left face) and perpendicular (right face) to stretching lineation, which is faintly visible as colour streaking on the top surface (weathered foliation). Note that the left face (parallel to the lineation) appears much more sheared than the other cut face: this can be a useful feature to look for on an irregular exposure when searching for stretching lineations. Line on top surface is part of the marking originally used to orientate the specimen. (Right face is 5 cm across.)
      • Figure 8.19 Clues to the stretching direction. (a) Dilational fractures perpendicular to a mineral lineation on this mylonitic foliation plane confirm the stretching direction, northwest India. (b) Composite sketch depicting clues to the stretching direction. ((a) Tom W. Argles, The Open University, UK.)
    • 8.3.3 Sense of shear: Kinematic indicators
      • Figure 8.20 Ductile kinematic indicators, all indicating dextral (‘top-to-the-right’) shear sense. (a) Asymmetric tails on feldspar porphyroclasts in a mylonite, northwest India. (b) Composite sketch depicting various features used for determining shear sense (width c. 40 cm). (c) S-C fabric (shear band cleavage) in a mica schist, Switzerland. Camera case near the base is 25 cm across. (d) Asymmetric pressure shadows on a boudin in a gneiss, northwest India. (a, c and d: Tom W. Argles, The Open University, UK.)
    • 8.3.4 Magnitude of shear strain
      • Figure 8.21 A deformed conglomerate showing flattening of pebbles that were probably much nearer spherical in the original sediment, Bhutan. (Tom W. Argles, The Open University, UK.)
    • 8.3.5 Fold analysis
      • Figure 8.22 Examples of different fold tightness. (a) An open fold in low-strain strata, near Minehead, Somerset, UK. (b) Tight folds indicating high strain are cross-cut by an undeformed (later) granite (top), Glen Gairn, Scotland. (c) Isoclinal folds show intense strain in metamorphosed mudstones (dark) and sandstones (pale brown), southern Spain. (d) Monocline in Carboniferous sedimentary rocks, Northumbria, UK. Hammer near centre for scale. (a and d: Angela L. Coe, The Open University, UK. b and c: Tom W. Argles, The Open University, UK.)
      • Figure 8.23 Examples of different fold shapes. (a) Chevron folds, common in uniformly layered strata at relatively shallow crustal levels, Tennessee, USA. (b) Disharmonic folds reflect contrasting rheologies of different layers. (c) Parallel folds imply competent layers. (d) Similar folds, with thickened hinge areas and thinned limbs, suggest weaker rocks that can deform easily. (a: Courtesy of the U.S. Geological Survey; Photographer W. B. Hamilton. b: Tom W. Argles, The Open University, UK.)
      • Figure 8.24 Information from fold asymmetry. (a) Schematic cross-section showing an example of how fold asymmetry (and vergence) changes across a fold axial plane (red line). (b) Isolated asymmetric fold in calcareous mylonite, implying dextral (top-to-the-right) shear, Switzerland. (Tom W. Argles, The Open University, UK.)
      • Figure 8.25 Approximations to fold axes. (a) Thin grooves and lines (parallel to yellow line) on dark-grey bedding plane are the intersection of cleavage with bedding. Bedding plane dips steeply to the left. Cleavage traces (parallel to red line) are visible in the vertical joint surface on the left of the photograph, cutting through steeply-dipping sedimentary layers (marked with green lines); west Wales, UK. (b) Diagram showing relationship of intersection lineations with a major fold structure; folded beds are shown in shades of brown. Intersections of cleavage on bedding are marked by dashed yellow lines on the folded, mid-brown bedding plane; intersections of bedding planes on cleavage (marked as dashed red lines) are shown on the steep cleavage plane on the left-hand side. The two lineations are both parallel to the fold axis. (c) Crenulation lineation, defined by the hinges of millimetre-scale folds, on the limb of a larger fold that is not visible in the field; Strath Fionan, Scotland. (a and c: Tom W. Argles, The Open University, UK.)
      • Worked Example 8.2 Unravelling multiple tectonic fabrics and folding
        • Figure 8.26 Page from a field notebook with sketch showing transposition of lithological layer in strongly deformed schists. (Notebook of Tom W. Argles, The Open University, UK.)
        • Figure 8.27 Sketch from a field notebook showing lower-strain zone near quartz vein where main foliation (S3) can clearly be seen to be a crenulation of an earlier schistosity (S2). (Notebook of Tom W. Argles, The Open University, UK.)
        • Figure 8.28 Sketch of albite porphyroblasts with curved, oblique included fabric, wrapped by foliation (S2) that is itself also tightly folded, with a weak axial-planar fabric (S3). (Notebook of Tom W. Argles, The Open University, UK.)
  • 8.4 Further reading
• 9 Recording features of metamorphic rocks
  • 9.1 Basic skills and equipment for metamorphic fieldwork
    • 9.1.1 Field relations and context
      • Worked Example 9.1 Mineral identification in southern Spain
        • Figure 9.1 Dark grey prisms in a fine-grained schist from southern Spain. Sample is c. 15 cm long.
        • Figure 9.2 Well-formed prisms in a synmetamorphic vein observed not far from the schist in Figure 9.1 show the characteristic pink colour of andalusite. These crystals lack the numerous graphite inclusions that give andalusite – and other porphyroblasts in the surrounding schists – a dull grey colour. (Tom W. Argles, The Open University, UK.)
  • 9.2 Textures
    • Figure 9.3 Interlayered metapelites and metapsammites, Spain. Metamorphic minerals have grown much coarser in the pelites (right half of view) than in the psammites (under lens cap), where quartz grains may even have been reduced in size due to recrystallization under strain. The relative grain sizes of the original sediments are thus reversed, and their colour and inferred compositions are much better guides to their protoliths than grain size. (Tom W. Argles, The Open University, UK.)
    • 9.2.1 Banding
      • Figure 9.4 (a) Gneissic banding defined by alternating felsic (pale) and mafic (dark) bands on a centimetre scale, northwest India. Subtler colour variation on a larger scale (5–10 bands width) suggests that the original precursor was compositionally layered (sedimentary or volcanic). Field of view is about 5 cm across. (b) Cross-stratification in metaquartzite picked out by colour bands caused by concentrations of heavy minerals; original younging direction is therefore to the right. Penknife at base for scale. (a and b: Tom W. Argles, The Open University, UK.)
    • 9.2.2 Grain textures
      • Figure 9.5 Grain textures. (a) Granular texture in a contact-metamorphosed hornfels, northern England. Cordierite grains have been weathered out, but the texture is preserved in the resistant quartz matrix. Field of view is 25 cm wide. (b) Granular texture in an eclogite-facies gabbro, where strain was partitioned into weaker rocks nearby; Switzerland. Field of view is 4 cm wide. (a and b: Tom W. Argles, The Open University, UK.)
    • 9.2.3 Reaction textures
      • Pseudomorphs
        • Figure 9.6 Reaction textures in the field. (a) Pseudomorphs of fine-grained white mica and clinozoisite (Ca,Al silicate) after lawsonite in a retrogressed blueschist, Switzerland. The lawsonite is inferred partly from crystal shape (rhombs). Largest rhombs are 5 mm across. (b) Corona texture in an eclogite, Switzerland. Thin red coronas of garnet separate white pseudomorphs of talc (after olivine) from pale bluish zoisite (after plagioclase) and green clinopyroxene. (a and b: Tom W. Argles, The Open University, UK.)
      • Coronas
      • Reaction zones
        • Figure 9.7 Metasomatic colour change (reddening) indicating fluid alteration either side of a crack. This rock was found adjacent to a fault zone with extensive reddening by haematite metasomatism. Field of view is 7 cm across. (Tom W. Argles, The Open University, UK.)
  • 9.3 Mineralogy
    • 9.3.1 Identifying common metamorphic minerals
      • Figure 9.8 Examples of common metamorphic minerals. (a) Typical rounded crystals of dark red garnet (Grt), wrapped by a tectonic fabric. Dark prisms with pointed ends are staurolite crystals (St), appearing black due to graphite inclusions. The crystal shape is a better diagnostic feature than colour. Staurolite is characteristic of iron-rich metasediments. (b) Biotite (Bt) and muscovite (Ms) are common as shiny, elastic flakes defining the foliation, as in this gneiss. Bright blue grains are small kyanite (Ky) crystals. (c) Three green minerals are associated with pale pink, Ca-garnet in this metabasic rock. The characteristically yellowish green mineral is epidote (Ep), which commonly occurs as aggregates. The dark green (almost black) mineral is the amphibole hornblende (Hbl). The other bluish-green mineral is chlorite (Chl), common in fine-grained, low-grade rocks. (d) The bladed shape of kyanite (Ky) is a reliable diagnostic feature. However, the striking blue colour displayed in this kyanite–biotite schist is commonly pale or absent in other examples of the mineral. (e) Fibrous masses of sillimanite with a pearly sheen are intergrown here with quartz, but often occur with biotite. (f) Prismatic amphibole crystals may show rhombic cross-sections in well-formed crystals. Amphiboles are widespread, and abundant in many mafic rocks. This dark green amphibole is actinolite (Act), intergrown with white mica. (g) Pyroxene generally appears duller than amphibole, and may show square or rectangular cross-sections. Pyroxene is characteristic of high-grade rocks. In this sheared gabbro, olive-brown pyroxene crystals (Px) have been altered during deformation to dark coronas of amphibole (Amph), forming eye-shaped features known as augen. (h) Cordierite (Crd) is usually found as indistinct ovoid blobs as here, looking almost like grease-spots or raindrops. Contrast these with the sharp outlines of andalusite (And) porphyroblasts in this hornfels. (i) Talc is so soft that it feels soapy. Here, talc (Tlc) forms ovoid pseudomorphs with a pearly sheen after olivine in a metagabbro, with thin garnet (Grt) coronas (pink), dark glaucophane (Na-amphibole; Gln), bright green omphacite (Na-pyroxene; Omph) and a pale groundmass of altered plagioclase.
    • 9.3.2 Using mineral assemblages
      • Table 9.1 Key minerals in common metamorphic rock compositions: L, low; M, medium; H, high; P, pressure; T, temperature.
    • 9.3.3 Classification of metamorphic rocks
  • 9.4 Unravelling metamorphism and deformation
    • 9.4.1 Pre-kinematic features
      • Figure 9.9 Pre-kinematic staurolite crystals strongly wrapped by a strong schistosity (orientated vertically). Some porphyroblasts (e.g. large crystal in centre) are flanked by strain shadows, mainly filled by a pale mineral. View about 7cm across. (Tom W. Argles, The Open University, UK.)
      • Figure 9.10 Sketches of mineral grains with different relationships to deformation. (a) Pre-kinematic, broken K-feldspar grains and a boudinaged tourmaline crystal (top right), wrapped by a high-strain foliation. (b) Syn-kinematic garnet with curved inclusion trails, showing inferred shear sense.
    • 9.4.2 Syn-kinematic features
      • Figure 9.11 Augen of pyroxene in metagabbro, with rims and tails of amphibole drawn out into the strong foliation. View about 12 cm across.
    • 9.4.3 Post-kinematic features
      • Worked Example 9.2 Charting the exhumation of subducted oceanic crust
        • Figure 9.12 Evidence that the metamorphosed rocks in the Zermatt area were once oceanic crust. (a) Deformed lozenges in a metabasalt, interpreted as pillows formed in a basalt erupted under water. The mineral assemblage indicates that these rocks were metamorphosed to eclogite facies, at depths of around 90 km (lens cap for scale at base of exposure). (b) Igneous mineralogy (plagioclase and pyroxene) metastably preserved in a metagabbro from the same area as the metabasalts in (a). The right-hand half of the field of view appears blurred because in this domain the original minerals have been partially altered to eclogite facies minerals, including garnet (red). View is about 6 cm across. (a and b: Tom W. Argles, The Open University, UK.)
        • Figure 9.13 Metamorphic textures from rocks in the Zermatt area. (a) Eclogite facies metagabbro, with green crystals of omphacite (Na-pyroxene) and coronas of red garnet encircling talc-rich pseudomorphs (after igneous olivine). Pale groundmass is altered plagioclase. View about 9 cm across. (b) Eclogite facies metagabbro with a weak blueschist facies foliation defined by dark blue amphibole, which wraps around pre-kinematic omphacite crystals (green). View is about 7 cm across. (a and b: Tom W. Argles, The Open University, UK.)
  • 9.5 Further reading
• 10 Making a geological map
  • 10.1 Principles and aims
  • 10.2 Preparation and materials
    • 10.2.1 Base maps and other aids
      • Topographic maps
        • Figure 10.1 Examples of topographic maps. (a) Extract of a 1:10,000 British Ordnance Survey map of part of Shropshire, UK showing field boundaries, tracks and buildings in detail. (b) Extract from 1:25,000 topographic map of part of southern Scotland, UK, from the British Ordnance Survey (within 10km grid square NX(25)35). Grid squares are 1 km across, and contour intervals are in metres. (c) Photocopy of part of a much smaller scale map of northern India, dating from the 1940s. Grid squares are 10,000 yards across, and contour intervals are in feet. Details are sparse for this large area and out of date, but such maps may be the best available in remote regions. (a: Ordnance Survey 1:10,000 Sheet SO38NE © Crown Copyright. b: Ordnance Survey 1:25,000 Scale Colour Raster © Crown Copyright 2009. An Ordnance Survey/EDINA supplied service.)
      • Aerial photographs
        • Table 10.1 Advantages and disadvantages of aerial photographs and satellite images for geological mapping.
      • Satellite images
      • Additional data
        • Worked Example 10.1 ASTER satellite mapping of rock units in southern Tibet
          • Figure 10.2 (a) Landsat image of part of southern Tibet, using bands 7, 5 and 3 (2.08–2.35μm, 1.55–2.75μm, 0.60–0.69μm wavelength respectively) to make a composite RGB image. Granites and gneisses in domes show up pale pink or beige, while metamorphic schists mantling the domes appear dark purple. Boxes show areas of images in part (b). (b) ASTER satellite images of the two boxed areas shown in (a). Granite appears red; gneisses appear pale blue; Palaeozoic schists appear dark blue to purple. (Landsat data in (a) courtesy of the U.S. Geological Survey/NASA; ASTER images in (b) from Watts et al. 2005.)
          • Figure 10.3 Detailed geological map of area shown in Figure 10.2b, drawn after ‘ground-truthing’ of ASTER images confirmed which rock type(s) gave which spectral response. ‘AEG’ and ‘DPP’ are two types of granite distinguished by field relations. (Modified from King 2007.)
    • 10.2.2 Equipment for mapping
      • Table 10.2 Summary of the equipment required for mapping (see also Tables 2.1–2.3).
      • Figure 10.4 (a) A home-made map case (c. 30 cm across) incorporating a rigid board for drafting, and a hinged Perspex sheet to protect map sheets without obscuring them. (b) A second map case, which has a clipboard base for A4-sized sheets. The hinge on the plastic cover is sprung so that it holds the position in the photograph unless secured; the side panels help protect the sheets from the elements, while allowing access to the field map.
  • 10.3 Location, location, location
    • 10.3.1 Equipment
    • 10.3.2 Using base maps
      • Worked Example 10.2 Trying triangulation
        • Figure 10.5 (a) Initial attempt at triangulating a location in a remote area with few suitable landmarks. The three plotted bearing lines meet in a triangle of error (shaded red), so the location is not determined very precisely. (b) Revised attempt at triangulating the location in (a). The fourth plotted bearing line (green) meets two of the previous lines in a smaller triangle of error, so the location is more precisely – and accurately – determined. (Base maps: Ordnance Survey 1:25,000 Scale Colour Raster from 10 km grid square NJ(38)30 © Crown Copyright 2009. An Ordnance Survey/EDINA supplied service.)
        • Table 10.3 List of landmarks and corresponding bearings used for initial triangulation attempt.
  • 10.4 Making a field map
    • 10.4.1 Information to record on field maps
      • Table 10.4 Checklist of information to be included on each field map.
      • Figure 10.6 A well-structured layout for additional information on a field map that contains most of the elements mentioned in Table 10.4, including a small graphic showing how this field map sheet relates to three adjacent sheets produced for the project. (Reverse side of field map of Angela L. Coe, The Open University, UK.)
      • Table 10.5 Information to record on a field map. Level of detail is determined by time allocated and scale of mapping. Conventional symbols used for plotting these data are given in Appendix A10 (Figure A10.3).
      • Figure 10.7 (a) A field map of an area in the English Lake District. Exposures are coloured, but not outlined or labelled with a unit code. Annotation is sparse, but includes some comments on vegetation and landscape features relevant to the underlying geology (depressions, scarps, marshy ground). (b) Magnified portion of an adjacent field map, showing a strike line symbol plotted at locality number 46. The strike line is accurately plotted, with a short tick indicating dip of the stratum to the southeast at 12°, and the exposure has been outlined using a thin black pen line. This map could be improved by using colour to distinguish mapping lines better from the base map, and by ringing the locality number for clarity. (c) A field map from a brief mapping exercise in Scotland. Locality numbers are ringed, and their location given by arrows. Detailed notes compete with structural symbols for space, and the map is rather congested. Such notes could be reserved for the field notebook alone in most mapping situations. (a and b: Extracts from field maps of Tom W. Argles, The Open University, UK. c: Extract from field map of Angela L. Coe, The Open University, UK.)
    • 10.4.2 The evolving map
      • Major lithological divisions
      • Lithological subdivisions and marker layers
    • 10.4.3 Sketch cross-sections
      • Figure 10.8 An example of a sketch section, redrawn from a notebook, based on observations of cleavage and bedding attitudes and minor fold structures on a road traverse in the northwest Himalaya. Numbers refer to localities. The kilometre-scale antiformal fold inferred here is a subordinate structure on the SW-dipping limb of a 20-km-scale syncline. (Tom W. Argles, The Open University, UK.)
  • 10.5 Mapping techniques
    • 10.5.1 Traverse mapping
      • Figure 10.9 River gorge at Wangtu, northwest India, illustrating the point that in very mountainous regions, the only practical mapping approach may be traverses along river sections or roads. In this view, the road is cut into the cliff on the left-hand side of the photograph, about half way up the image. (Tom W. Argles, The Open University, UK.)
      • Linear traverse
        • Figure 10.10 (a) A linear traverse mapped in the Alaknanda valley, northwest India. In this complex orogenic zone, the focus of this project was on gathering structural data and collecting samples for metamorphic and geochemical analysis. (b) Correcting a closed compass traverse for minor bearing errors. When the traverse was plotted using the bearings and distances in the notebook (red lines), the last leg (e to a) did not join up exactly to the origin (Point A), by a closure error of 43 m. The traverse was corrected by adjusting each plotted point (a to e) parallel to the closure error (green lines) by an amount proportional to the cumulative distance travelled to reach that point. So, for point d, correction = 43 × (780/1435) = 23.4 m. The result is the corrected closed traverse ABCDE (dashed blue lines).
      • Closed compass traverse
    • 10.5.2 Contact mapping
      • Figure 10.11 Contacts like this one in southern Tibet may be conspicuous enough to be traced across difficult terrain using binoculars. (Tom W. Argles, The Open University, UK.)
    • 10.5.3 Exposure mapping
      • Figure 10.12 (a) An example of a field map produced by exposure mapping, with exposures outlined in pen; note that unit boundaries are also shown as dashed or solid lines. (b) A portion of the final fair copy map from the field map in (a), showing how the inferred outcrops of the mapped units are shown as solid blocks of colour. (Field map and final fair copy map of Susie Clarke, Oxford, UK.)
    • 10.5.4 Using other evidence
      • Topographic features: Feature mapping
        • Figure 10.13 (a) Part of a field map of the Long Mynd area, Shropshire, UK, incorporating landscape features (e.g. breaks in slope) as evidence of stratigraphic boundaries. Each break in slope is marked as a line with a series of arrows pointing at it; two occur in the centre of this extract, with another at top right. Superficial deposits that obscure the bedrock geology are also mapped. (b) The corresponding portion of the final fair copy map from the field map in (a), showing how the inferred outcrop of the bedrock units is depicted; the two central breaks in slope mark the boundaries of the Hillend Grit. (Field map and final fair copy map of Angela L. Coe, Open University, UK.)
        • Table 10.6 Topographic clues to bedrock geology.
        • Figure 10.14 Some landscape clues to bedrock geology. (a) Two breaks in slope (arrowed) mark the boundaries between massive gabbro (crags on left) and cleaved mudstones (underlying fields on right) at Carn Llidi, southwest Wales, UK. The intermediate slopes are underlain by contact metamorphosed mudstones and gabbro debris. (b) Steep scarp slopes mark resistant strata, near Haltwhistle, UK: a sandstone at A and the Whin Sill (dolerite sill) at B and C. The horizon dipping to the right (south) follows the dip of the sill. Depressions between the scarps are underlain by softer siltstones and limestones. (a and b: Tom W. Argles, The Open University, UK.)
      • Drainage
        • Figure 10.15 Examples of drainage and vegetation contrasts. (a) Marshy ground with rushes (foreground) marks the outcrop of impermeable Silurian mudstones, while most of the sheep are grazing on the well-drained pasture underlain by permeable Carboniferous Limestone (exposed in the crags behind). The contact between the two rock types is marked by a distinct break in slope, conspicuous against the woodland near the left-hand side of the photograph. Witherslack, Cumbria, UK. (b) The green verdant vegetation and flatter foreground is underlain by interbedded limestones and mudstones. The steeper slopes with vegetation typical of acidic soils (heather, bracken) are underlain by sandstone. The contact is marked by the vegetation change, running from just left of the group of trees on the horizon obliquely left behind the plantation on the left-hand side. This locality is near Alnwick, Northumberland, UK. (a: Tom W. Argles, The Open University, UK; b: Angela L. Coe, The Open University, UK.)
        • Table 10.7 Drainage characteristics of the underlying geology.
      • Soils and vegetation
        • Figure 10.16 (a) White fragments of chalk in this soil are a conspicuous clue to the bedrock beneath. It is always worth checking soil excavated by burrowing organisms (in this case prairie dogs at Whipsnade Zoo, Bedfordshire, UK). Burrow is about 12 cm across. (b) A hand auger, useful for obtaining samples of the shallow subsurface, including soil. The auger is lying alongside a loose ‘core’ of soil obtained from this locality. (a: Tom W. Argles, The Open University, UK; b: Mark Brandon, The Open University, UK.)
      • Superficial deposits
        • Figure 10.17 Typical landslide topography in Glacier National Park, Montana. The landslide material forms the hummocky ground with patchy vegetation sloping from the scree fans at the base of the cliffs towards the level plain in the foreground. (Courtesy of the U.S. Geological Survey; photographer P. Carrara.)
        • Figure 10.18 Field map in an area of poor exposure, with annotations on auger borings of the shallow subsurface augmented by notes on breaks in slope. Most boundaries are dashed or dotted (inferred). Auger holes are marked with a plus symbol (+); actual exposures are marked with a star (*); letters refer to notebook entries. (Map of Kate J. Andrew, Herefordshire Heritage Service, UK.)
  • 10.6 The geological map
    • 10.6.1 Inking in the field map
    • 10.6.2 Cross-sections
      • Figure 10.19 Stages in drawing a geological cross-section. (Map for b and d: Ordnance Survey 1:25,000 Scale Raster © Crown Copyright 2009. An Ordnance Survey/EDINA supplied service. Geological Map Data © NERC 2009.)
    • 10.6.3 Fair copy maps
      • Figure 10.20 An example layout for a fair copy map. (Map of Angela L. Coe, The Open University, UK.)
      • Table 10.8 Methods for transferring lines to a fair copy map.
      • Table 10.9 Additional elements of a final fair copy map.
    • 10.6.4 Digital maps and GIS
  • 10.7 Further reading
• 11 Recording numerical data and use of instruments in the field
  • Table 11.1 Commonly used equipment, main use and examples.
  • 11.1 Data collection
    • Figure 11.1 Some examples of the recording of numerical data in a field notebook. (a) Gamma-ray spectrometer data from five sample points (stations), showing stratigraphic position, raw and processed data and electronic file reference (pos). In this case gamma-ray spectrometer readings were taken every 30 cm (i.e. every third station, in order to match with the resolution of the instrument; other readings were taken every 10 cm). (b) Magnetic susceptibility data every 2.5 cm (whole-number stations are every 10 cm), background readings in air and two readings on the rock. This instrument measures continuously and integrates the data to provide a reading every 10 seconds. The small black circles represent readings given by the instrument as it is moved from rock to air. The recording of this as a point ensures that there is no mistake made between these meaningless measurements and the data required. (Notebooks of Angela L. Coe, The Open University, UK.)
    • Figure 11.2 (a) Three-dimensional representation of the bell-shaped volume (shown in red) over which the gamma-ray spectrometer measures. Two-dimensional representation of the area that the instrument will detect if used (b) parallel to the bedding plane, (c) perpendicular to bedding or (d) at an angle.
    • 11.1.1 Instrument calibration and base stations
    • 11.1.2 Survey grids
  • 11.2 Transport and protection of the instruments
  • 11.3 Correlation with other data sets
  • 11.4 Further reading
• 12 Photography
  • Figure 12.1 Two photographs taken under slightly different f-stops to illustrate the effect of varying the camera settings. Images are 40 cm high. (a) f 6.3 and (b) f 4.5. The associated metadata that it is useful to include in an electronic file are: camera type, shutter speed, f-stop, ISO setting, white balance (see Figure 12.2), focal length, date, time, place, subject, keywords. Some of this is recorded automatically and other parts such as the subject matter need to be added by the user. (a and b: Angela L. Coe, The Open University, UK.)
  • Figure 12.2 Two images of grey mudstones from the Monterey Formation, California, USA showing the large colour difference when using a different white balance setting. Images are 1 m high. (a) Auto setting. (b) After using a white balance card to adjust the balance for the lighting conditions (seek advice from professional photographer/photographic shop). All other camera light settings are exactly the same. (a and b: Angela L. Coe, The Open University, UK.)
• 13 Sampling
  • 13.1 Selecting and labelling samples
    • 13.1.1 Samples for thin-sections
    • 13.1.2 Orientated samples
      • Younging direction and approximately orientated samples
      • Precisely orientated samples
        • Figure 13.1 Orientated sample with combined strike line and direction of dip on the top surface and the sample number (H01) and way up (arrow) on the side. In this case part of the limestone that is fractured but nevertheless still intact and orientated has been chosen. Carboniferous strata, Rumbling Kern, Northumberland, UK. (a and b: Angela L. Coe, The Open University, UK.)
    • 13.1.3 Samples for geochemical analysis
    • 13.1.4 Samples for mineral extraction
    • 13.1.5 Samples for fossils
    • 13.1.6 Sampling for regional studies
    • 13.1.7 High-resolution sample sets
      • Figure 13.2 Marked sections ready for sampling. Lower Jurassic, Yorkshire, UK. (a) One stratigraphic metre of rock marked every 1 cm. (b) Detail section showing marks every 1 cm made with a tile scribe and correction fluid. Note in this case the letter ‘m’ indicates minus as the marks are below the zero reference datum shown in (a). (c) Marking sections on both sides of a corner can be helpful when putting the section back together. (a–c: Christopher Pearce, The Open University, UK.)
    • 13.1.8 Labelling samples and their packaging
  • 13.2 Practical advice
    • 13.2.1 Packing and marking materials
    • 13.2.2 Extraction of samples
• 14 Concluding remarks
  • Table 14.1 Summary of information to consider recording in your field notebook.
  • 14.1 Further reading on scientific report writing
• Back Matter
  • References
  • Appendix A1: General
    • Figure A1.1 Chart to estimate percentage composition from area.
    • Table A1.1 Mohs’ scale of hardness.
    • Table A1.2 Metric to Imperial length conversion chart.
    • Table A1.3 Natural sines for conversion of horizontal measurements to true thickness (see Section 2.5.1).
    • Geological timescale
  • Appendix A5: Fossils
    • Table A5.1 Modes of fossil preservation.
    • Figure A5.1 A simple scheme for the identification of invertebrate fossils based on symmetry.
    • Figure A5.2 Diagram illustrating the formation of moulds and casts using a bivalve as an example.
    • Figure A5.3 Illustrations of some common trace fossils. ((a)–(j) Angela L. Coe, The Open University, UK. Except (f) plan view; Fiona Hyden, Open University Associate Lecturer, UK.)
    • Table A5.2 There has been a plethora of categories for classifying trace fossils. One such classification is based on the interpretation of what the animal was doing. Note that many of these are not mutually exclusive.
    • Figure A5.4 Examples of tiering of burrows and their implications. (Modified after Goldring 1991.)
    • Figure A5.5 Biostratigraphically useful groups of organisms. The thick part of the line indicates the interval where the fossil group is used most extensively. (Modified after Nichols 1999 and Emery and Myers 1996.)
    • Figure A5.6 The common zonation schemes used in biostratigraphical correlation. (Modified after Nichols 1999.)
  • Appendix A6: Sedimentary
    • Table A6.1 Checklist for the description of sedimentary deposits.
    • Table A6.2 Features of common minerals that constitute sedimentary deposits.
    • Table A6.3 Types of common coals and their depositional environment.
    • Table A6.4 Ripples are common in the sedimentary record. This table indicates how to distinguish current-formed ripples diagnostic of linear fluid flow from wave-formed ripples diagnostic of the orbital motion of waves produced by wind blowing over standing bodies of water.
    • Distinguishing between micrite and sparite
      • Figure A6.1 Grain-size descriptors.
      • Figure A6.2 Comparison charts for particle sorting.
      • Figure A6.3 Comparison charts for grain morphology. (a) Rounding and sphericity. (b) Shape.
      • Figure A6.4 Comparison charts for grain fabric. It is also appropriate to note whether the grains are aligned if they are tabular of bladed.
      • Figure A6.5 Terms for the description of lamination/bed thickness, etc.
      • Figure A6.6 Terms for the description of bed character.
      • Figure A6.7 Different types of sedimentary grading.
      • Figure A6.8 Classification of sandstones. (Modified after Pettijohn et al. 1973.)
      • Figure A6.9 Classification of mudstones. (Modified after Stow 2005.)
      • Figure A6.10 Main limestone-forming grains.
      • Figure A6.11 Folk scheme for the classification of limestones. (Modified after Folk 1962.)
      • Figure A6.12 Dunham scheme for the classification of limestones. (Modified after Dunham 1962 with additions from Embry and Klovan 1971.)
      • Figure A6.13 Classification of coarse-grained sedimentary rocks (conglomerates, breccias, etc.). Modified after Boggs 1992, Nichols 1999 and Stow 2005. In addition the following terms can be applied: intraformational conglomerate and breccia, composed of clasts of the same material as the matrix; extraformational conglomerate, composed of a mixture of rock types; clast-supported (or orthoconglomerate); matrix-supported (or paraconglomerate or diamictite).
      • Figure A6.14 Sketch illustrating the spectrum of coastal morphological features and the processes dominant in each case. The importance of waves, tides and fluvial input is shown schematically by the boxes at the top of each figure; tapering of the box indicates less influence of that process.
      • Figure A6.15 Sequence stratigraphy summary figures. (a) Idealized illustrations of key features of the sequence stratigraphy model on the relative sea-level curve for (b) to (e), showing the position of the systems tracts and key surfaces. In this example, parasequences are assumed to have equal duration as indicated by the equal time units t0, t2, etc. (b and d) Cross-sections through a HST and the overlying depositional sequence (FSST, LST, TST and HST) for a continental margin with a shelf break (b) and ramp type continental margin (d). (c and e) Chronostratigraphical representation of (b) and (d) respectively. Hemipelagic and pelagic sediments are not shown. (From Coe 2003.)
      • Figure A6.16 Some of the commonly used symbols for graphic logs and some ideas for other more specific features.
      • Figure A6.17 Common sedimentary structures. See also Tables 6.2–6.4. Red penknife is 9 cm long. (All Angela L. Coe, The Open University, UK, except (x) and (cc), R. Chris L. Wilson.)
  • Appendix A7: Igneous
    • Table A7.1 Names for igneous intrusions, based on shape and relationship with country rocks.
    • Table A7.2 Typical properties, visible in hand specimen, of common minerals that may be found in igneous rocks.
    • Figure A7.1 Classification scheme for igneous rock types, by grain size and mineralogy. Fine-grained felsic rocks are paler than fine-grained mafic rocks, and may be reddened by alteration. However, glassy rhyolite (obsidian) can be black.
  • Appendix A8: Structural
    • Figure A8.1 Diagram of an oblique-slip fault, annotated with terms for its main components. The actual displacement (green arrows) can be divided into two components: dip-slip component (ds) and strike-slip component (ss).
    • Figure A8.2 Diagram of a typical fold pair, labelled with terms for the main parts of fold structures. The terms antiform and synform describe the form of the folds. If the sequence is right-way up (i.e. the stippled layer is younger than the pale blue layer), then the antiform is an anticline, and the synform is a syncline.
    • Figure A8.3 Schematic illustration of different types of fold tightness, defined according to the angle between the two fold limbs (the interlimb angle). (Based on Fleuty 1964.)
    • Figure A8.4 Classification of fold types using a combination of the dip of the axial plane and the plunge of hinge line.
    • Figure A8.5 Block diagrams illustrating several different types of lineations. (a) Striations (slickenlines) on a fault plane. (b) Stretching lineation defined by deformed (elongated) mineral grains. (c) A rock with both foliation (flattening) and lineation (stretching). (d) Crenulation lineation defined by the hinge lines of microfolds. (e) Intersection lineations in a fold. Two different lineations are shown: the intersection of cleavage on a folded bedding plane, and the intersection of cleavage on a joint plane. (Modified from Park 1989.)
    • Figure A8.6 The Flinn diagram uses measurements of the principal strain axes in deformed rocks to distinguish constrictional from flattening strains. The equiline (k = 1) bisecting the plot represents plane strain. Rxy and Ryz are the principal plane strain ratios, calculated from the principal longitudinal strains e1, e2 and e3. (Modified from Ramsay and Huber 1984.)
    • Table A8.1 Textural classification of fault rocks based on Sibson 1977.
    • A note on stereographic projections
  • Appendix A9: Metamorphic
    • Table A9.1 Properties useful for field identification of some common metamorphic minerals. Mohs’ scale of hardness (H) is given in Appendix A1, Table A1.1.
    • Figure A9.1 The metamorphic facies diagram, dividing P–T space into different fields characterized by particular mineral assemblages in mafic rocks. The wet melting curve for granite is also shown, and the approximate region of Barrovian metamorphic assemblages is outlined (dashed line).
    • Figure A9.2 A map of the Scottish Highlands, showing the distribution of Barrow metamorphic zones (and the low-pressure Buchan andalusite zone in the northeast). One of the classic transects where the metamorphic zones were first mapped by George Barrow, Glen Esk, is marked by the line XY.
  • Appendix A10: Mapping
    • Determination of true and apparent dip
      • Figure A10.1 Nomogram to determine the apparent dip given the true dip and the angle between the strike and the line of section. The dashed line illustrates an example: for a true dip of 43° on a cross-section oriented at 35° to the strike of the bedding, the apparent dip on the cross-section would be 28°. (Based on Billings 1972.)
      • Figure A10.2 A graph to determine the apparent dip angles (solid, curved lines) and the thickness exaggeration (curved blue lines) for bedding in cross-sections that are not parallel to the true dip direction (i.e. where the strike of bedding is not perpendicular to the line of section). An example is given on the diagram (red lines) for bedding with a true dip of 45° on a cross-section orientated at 60° to the dip direction. In this case, the apparent dip of 27° can be read off the graph, and the thickness of bedding will be 1.275 times the actual thickness. (Modified from McClay 1991.)
      • Figure A10.3 A selection of symbols for use in preparing geological maps. Alternatives are given for some of the symbols.
  • Index

  UM RAFBÆKUR Á HEIMKAUP.IS

  Bókahillan þín er þitt svæði og þar eru bækurnar þínar geymdar. Þú kemst í bókahilluna þína hvar og hvenær sem er í tölvu eða snjalltæki. Einfalt og þægilegt!
  
  Rafbók til eignar
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  Þú kemst í bækurnar hvar sem er
  Þú getur nálgast allar raf(skóla)bækurnar þínar á einu augabragði, hvar og hvenær sem er í bókahillunni þinni. Engin taska, enginn kyndill og ekkert vesen (hvað þá yfirvigt).
  
  Auðvelt að fletta og leita
  Þú getur flakkað milli síðna og kafla eins og þér hentar best og farið beint í ákveðna kafla úr efnisyfirlitinu. Í leitinni finnur þú orð, kafla eða síður í einum smelli.
  
  Glósur og yfirstrikanir
  Þú getur auðkennt textabrot með mismunandi litum og skrifað glósur að vild í rafbókina. Þú getur jafnvel séð glósur og yfirstrikanir hjá bekkjarsystkinum og kennara ef þeir leyfa það. Allt á einum stað.
  
  Hvað viltu sjá? / Þú ræður hvernig síðan lítur út
  Þú lagar síðuna að þínum þörfum. Stækkaðu eða minnkaðu myndir og texta með multi-level zoom til að sjá síðuna eins og þér hentar best í þínu námi.
  
  
  
  Fleiri góðir kostir
  - Þú getur prentað síður úr bókinni (innan þeirra marka sem útgefandinn setur)
  - Möguleiki á tengingu við annað stafrænt og gagnvirkt efni, svo sem myndbönd eða spurningar úr efninu
  - Auðvelt að afrita og líma efni/texta fyrir t.d. heimaverkefni eða ritgerðir
  - Styður tækni sem hjálpar nemendum með sjón- eða heyrnarskerðingu