A Color Illustrated Guide to Carbonate Rock Constituents, Textures, Cements, and Porosities (AAPG Memoir 27)

Memoir 27

A Color Illustrated Guide To

Carbonate Rock Constituents, Textures, Cements, and Porosities

Peter A.Scholle U.S. Geological Survey

Published by The American Association of Petroleum Geologists with the support of The American Association of Petroleum Geologists Foundation Tulsa, Oklahoma, U.S.A., 1978

Introduction

The purpose of this book is to make available to geologists who may not be specialists in carbonate petrography a volume which illustrates the major grains, textures, cements, and porosity types found in carbonate rocks. Successful hydrocarbon exploration in carbonate rocks is a difficult and complex problem. Carbonate rocks not only have complicated and varied depositional patterns, but also are subject to extensive post-depositional alteration which may radically alter original porosity and permeability relationships. Because these diagenetic changes can occur at many stages of burial and(or) uplift, the timing of such events relative to hydrocarbon migration and structural deformation is important. Petrography commonly is the most valuable tool which can be used to resolve such interpretational problems in potential reservoir rocks. This book is designed as an introduction for the explorationist or student, and is by no means a complete treatise or textbook. However, it does include a wide variety of examples of skeletal and nonskeletal grains, cements, fabrics, and porosity types. It also encompasses a number of noncarbonate grains which can occur as common accessory minerals in carbonate rocks or which may provide important biostratigraphic or paleoenvironmental information in carbonate rocks. With this guide, people with little formal training in petrography should be able to examine thin sections or peels under the microscope and interpret the main rock constituents and their depositional and diagenetic history. Carbonate petrography, because it involves very few minerals (mainly calcite with subordinate dolomite, quartz, and clay), is primarily a qualitative art. One must learn to recognize the distinguishing characteristics of skeletal grains of various ages. Different directions of sectioning will produce radically different appearances, as will different stages of diagenetic alteration. There are no simple diagnostic tests (such as measuring birefringence, optic figure, etc.) which will absolutely identify a bryozoan, for example. It is simply a question of experience. Comparison of grains in thin sections with photographs of identified grains in this and other books will quickly allow geologists to correctly identify the majority of the rockforming grains in their samples. A selected bibliography is provided to permit the interested reader to pursue details only briefly covered in this book and, particularly, to supplement the interpretive aspects of petrographic work. A particular attempt has been made to illustrate typical rather than spectacular examples of many grains and fabrics. For example, grains which were originally composed of aragonite normally undergo wholesale diagenetic alteration which commonly obliterates primary structural features. Therefore, such grains are shown in their extensively altered state because this preservation is typical. A table of original mineralogies is provided to help the reader anticipate preservation problems. Furthermore, examples have been included from rocks of Cambrian to Holocene age because of the enormous evolutionary changes in organisms (and, therefore, carbonate fabrics) through time.

IV

In terms of the overall costs of hydrocarbon exploration today, the financial investment needed for petrographic work is virtually insignificant. A basic polarizing microscope can be purchased currently for $1,000 to $5,000 depending on optical quality, accessories, and other factors. Thin sections can be purchased for $2 to $5 each from a number of commercial labs. Acetate peels (see technique section of the bibliography) can be made in any office in minutes from polished rock slabs, and can provide a remarkable amount of information. Outcrop samples, conventional cores, sidewall cores, and cuttings samples all can be examined microscopically although textural information decreases with decreasing sample size. Even the investment of time involved in petrographic work need not be great relative to the potential for problem solving. Few other techniques are as valuable and accurate for the identification of preserved, destroyed, or created porosity, or the prediction of depositional and diagenetic trends. Research conducted over the past 25 years has outlined many principles of deposition and diagenesis in carbonate sediments. Facies models have been established for modern (as well as ancient) reefs and other bank-margin deposits, for tidalflat and sabkha sedimentation, for basinal deposition, and for other environments. Diagenetic studies have pointed out the influence of syndepositional marine cementation, early freshwater diagenesis, and later subsurface compaction-dissolution phenomena. This work has clearly shown that, although carbonate depositional and diagenetic patterns may be complex, there is commonly a large volume of information recorded in the rocks which can be used to decipher this record. For example, virtually all carbonate grains are produced either directly by, or through the indirect influence of, organisms. Unlike clastic terrigenous particles, carbonate grains are rarely transported far from their original site of formation. Thus, the identification of a biologically produced suite of grains will often reveal considerable information about the environment of deposition. Likewise, marine, freshwater, and late subsurface cements each have distinctive, recognizable fabrics. Petrography, when used in close conjunction with well-log analysis, seismic interpretation, regional geology, and other studies, can be an invaluable tool for applying these recently developed principles of carbonate sedimentology to ancient rocks. Furthermore, it is best applied by the explorationist who is deeply involved in techniques other than petrography, for he is in the best position to ask the right questionsquestions petrography may be able to answer. That is the goal of this volume.

(including geologic age) and state or country of origin. This is followed by a description of the photograph. The last line of the caption defines the type of lighting used and the scale of the photograph. The following code is used for lighting: X.N.—crossed nicols (cross-polarized light) P.X.N.—partly crossed nicols G.P.—gypsum plate (Quartz Red I plate) inserted R.L.-reflected light The absence of any symbol indicates that transmitted light with uncrossed polarizers was used. All scales are given as a certain number of millimeters (or micrometers jum, for scanning electron microscopy, SEM) for a scale bar of uniform length (1.25 cm or 0.5 inches) for all photographs. Thus, a figure of 0.38 mm indicates that a length of 1.25 cm on the printed picture is equivalent to 0.38 mm on the original specimen.

Acknowledgements An earlier version of this book was compiled at Cities Service Oil Company Research Laboratory and much of that original version is included here. I would like to express my great appreciation to Cities Service for their kind permission, even encouragement, to publish this volume. During the seven years of its existence, this book (in various unpublished editions) has been reviewed or commented upon by hundreds of persons and it has grown largely through the contribution of samples by persons too numerous to mention. Thanks also go to R. M. Forester, R. B. Halley, and N. J. Silberling who reviewed copies of this book; J. P. Bradbury, R. N. Ginsburg, and W. J. Meyers who kindly contributed photographs; and L. R. Tomlinson and J. L. Hennessy who greatly aided in the editorial preparation of this volume. Finally, I would like to express my appreciation to the three petrographers who spent many hours looking down a microscope with me and whose teaching dedication made this volume possible: R. G. C. Bathurst, A. G. Fischer, and R. L. Folk.

35mm Slides Available A set of 100 selected photographs from this book are available in 35 mm slides. The set is designed to aid instructors who might use the text for teaching purposes. To order the set, or to request a free brochure, contact: AAPG Publications, P.O. Box 979, Tulsa, Oklahoma 74101.

Explanation of Captions

A similar set of slides for clastic rocks keyed to AAPG Memoir 28, " A Color Illustrated Guide to Constituents, Textures, Cements, and Porosities of Sandstones and Associated Rocks," also is available from AAPG.

Each photograph in this manual has a description in standard format. The first two lines give the stratigraphic unit

V

Biolithite limestone made up of organic structures growing in place and forming a coherent, resistant mass during growth (Folk, 1959, 1962). Biomicrite limestone composed of skeletal grains in a micrite matrix (Folk, 1959, 1962). Biosparite limestone composed of skeletal grains with sparry calcite cement (Folk, 1959, 1962). Bladed in reference to sparry calcite cement, defined as including crystals with a length-to-width ratio between 1.5:1 and 6 : 1 . Borings openings created in relatively rigid rock, shell, or other material by boring organisms. The rigid host substrate is the feature which distinguishes borings from burrows; the latter form in unconsolidated sediment. Boundstone carbonate rock showing signs of grains being bound (by organisms) during deposition (Dunham, 1962).

Glossary: Carbonate Petrography

Calcarenite limestone composed predominantly of sand-sized calcium carbonate grains (carbonate sand). Calcilutite mud).

(Source references given o n l y

limestone composed of lithified calcareous mud (lime

Calcirudite limestone composed predominantly of calcium carbonate fragments larger than sand size (carbonate conglomerate).

f o r carbonate rock classification)

Calcispheres silt- or sand-sized spheres of clear (sparry) calcite, some with a discernible wall and some without . Probably of diverse origin, algal spores being a likely major variety. Calclithite a rock formed chiefly of carbonate clasts derived from older, lithified limestone, generally external to the contemporaneous depositional system. Commonly formed along downthrown sides of fault scarps. Caliche (calcrete) surficial material such as sand, gravel, or cobbles cemented by calcium carbonate in arid climates as a result of evaporative concentration of CaCOg in surface pore waters. Often characterized by crusts, pisolites, reverse grading, autofracturing, and microstalactitic textures.

Allochems an inclusive term for carbonate grains or particles, as contrasted to carbonate mud matrix and clear calcite cement; includes fossils, oolites, pellets, etc. (Folk, 1959, 1962).

Cavernous Porosity a pore system characterized by large openings or caverns. Such porosity is too large to be identified in normal subsurface cores but is recognizable during drilling by large drops (0.5 m or greater) of the drill bit.

Anhedral a single crystal or crystal fabric which does not show well-defined typical crystallographic forms. Bahamite granular limestone resembling the Holocene deposits in the Bahamas; composed largely of pellet-like aggregates of carbonate mud.

Chalk a limestone which consists predominantly of the remains of calcareous nannoplankton (especially coccoliths) and microplankton (especially Foraminifera). Chalks are often considered to be soft and friable, although diagenetic alteration can lead to complete lithification of chalks.

Beach Rock a friable to well-cemented rock consisting of calcareous sand cemented by calcium carbonate crusts precipitated in the intertidal zone. Generally found as thin beds dipping seaward at less than 15°.

Clastic as used by most sedimentary petrologists, composed of particles that have been mechanically transported, at least locally. Specifically includes limestones made up of fossils or other allochems that have been moved by waves or currents. (Note that most facies mappers use clastic for terrigenous rocks and not limestones).

Biochemical deposited by chemical processes under biologic influence. For example, the removal of CO2 from sea water by aquatic plants may cause calcium carbonate to precipitate.

VI

Coated Grains a general term for grains with coatings or rims of calcium carbonate; includes oolites and superficial oolites, pisolites, and algal-coated grains.

Interstices technically, voids; but used mostly for areas that were voids in the initial sediment, though they are now filled. Intraclast a fragment of penecontemporaneous, commonly weakly consolidated, carbonate sediment that has been eroded from sea bottom and redeposited nearby.

Detrital used in different ways by different authors and hence undefinable out of context. Sometimes synonymous with clastic, sometimes with terrigenous, and sometimes restricted to rocks composed of broken older rocks.

Isopachous (grainskin) a descriptive term for cement which has formed as a uniform-thickness coating around grains. Common in most submarine cements.

Diagenesis changes in sediments or sedimentary rocks which occur after deposition but excluding processes involving high enough temperature and pressure to be called metamorphism.

Lithographic refers to extremely fine and uniform carbonate usually with smooth conchoidal fracture.

Dismicrite disturbed micrite; a carbonate mud that contains stringers or "eyes" of sparry calcite resulting from filling of burrows, slump or shrinkage cracks, or other partial disruption on the sea floor (Folk, 1959, 1962).

Lumps in modern sediments, irregular composite aggregates of silt- or sand-sized carbonate crystals that are cemented together at points of contact: in ancient carbonates, similar-appearing grains composed of carbonate mud.

Eogenetic occurring during the time interval between final deposition and burial of the newly deposited sediment or rock below the depth of significant influence by processes that either operate from the surface or depend for their effectiveness on proximity to the surface.

Meniscus refers to a carbonate cement type formed during vadose diagenesis where cement crystals form only at or near grain contacts in the positions a water meniscus would occupy. Mesogenetic occurring during the time interval in which rocks or sediments are buried at depth below the major influence of processes directly operating from or closely related to the surface.

Equant in reference to sparry calcite cement it is defined as including crystals with a length to width ratio of less than 1.5:1. Euhedral refers to a single crystal or crystal fabric which shows well-defined typical crystallographic forms.

Micrite microcrystalline calcite; used both as a synonym for carbonate mud (or "ooze") and for a rock composed of carbonate mud (calcilutite) (Folk, 1959,1962).

Extraclast a detrital grain of lithified carbonate sediment (lithiclastl derived from outside the depositional area of current sedimentation. The rock composed of these grains would be a calclithite. See also intraclast.

Microspar generally 5- to 15-micron sized calcite produced by recrystallization of micrite; can be as coarse as 30 microns (Folk, 1965). Microstalactitic (pendulous or gravitational cement) a descriptive term for cements which are concentrated on the bottom sides of grains. Such textures generally form in vadose or upper intertidal areas where pores are only partially water-filled and in which water droplets can hang from the undersides of grains.

Fenestrae (fenestral fabric) primary or penecontemporaneous gaps in rock framework larger than grain-supported interstices. Commonly associated with algal mats and can result from shrinkage, gas formation, organic decay, etc. Fibrous in reference to sparry calcite cement it is defined as including crystals with length-to-width ratios greater than 6 : 1 .

Mold a pore formed by the selective removal, normally by solution of a former individual constituent of the sediment or rock such as a shell or ooid. Often used with modifying prefixes: oomoldic, dolomodic, etc.

Geopetal Structure any internal structure or organization of a rock indicating original orientation such as top and bottom of strata.

Mudstone in referring to carbonates, a carbonate rock composed of carbonate mud with less than 10% allochems (Dunham, 1962).

Grains (11 solid particles whose physical limits may encompass many crystalline entities. Distinctions as between coarse grained and coarsely crystalline are not always observed but are fundamental; 12) the friable aggregates of silt-sized carbonate crystals that are forming today on the Bahaman Platform from the partial cementation of crystals in contact with each other.

Oncolite a pisolite of algal origin a spheroidal form of algal stromatolite showing a series of concentric (often irregular) laminations. These unattached stromatolites are produced by mechanical turning or rolling, exposing new surfaces to algal growth. Oolite (ooids) Oolite is a rock composed of ooids. Ooids are spherical to ellipsoidal bodies, 0.25 to 2.00 mm in diameter with a nucleus and radial or concentric structure (calcareous, hematitic, siliceous, etc.) generally grown in an agitated environment.

Grain-supported refers to the fabric of a rock in which the grains (allochems) are in contact with each other, even though they may have a mud (micrite) matrix. Grainstone carbonate rock composed of grains with no carbonate mud in the interstices (Dunham, 1962).

Oomicrite a limestone composed dominantly of ooids in a matrix of micrite (Folk, 1959, 1962).

Grapestone sometimes used for aggregates of silt-sized carbonate crystals (grains, def. 2), but more properly applied to grape-like clusters of such aggregates.

Oosparite a limestone composed dominantly of ooids in sparry calcite cement (Folk, 1959, 1962).

VII

Ooze carbonate mud; either the original soft sediment or its consolidated equivalent.

Secondary Porosity deposition.

Orthochemical a rock constituent that is a normal chemical precipitate, as contrasted to fossils, oolites, or other mechanically or biologically deposited constituents.

Shelter Porosity a type of primary interparticle porosity created by the sheltering effect of relatively large sedimentary particles which prevent the infilling of pore space beneath them by finer clastic particles.

Packed containing sufficient grains (allochems) for the grains to be in contact and mutually supporting, as contrasted with rocks with grains "floating" in mud (Folk, 1959, 1962).

Skeletal Carbonate components (or the rocks they form) derived from hard material secreted directly by organisms. A substitute for the confusing term organic of some older literature.

Packstone carbonate rock composed of packed grains with carbonate mud matrix (cf. grainstone and wackestone; Dunham, 1962).

Spar (sparry calcite) calcite sufficiently coarsely crystalline to appear fairly transparent in thin section, as contrasted to dark, cloudyappearing carbonate mud or micrite (Folk, 1959, 1962).

any porosity created in a sediment after final

Pellet a grain composed of micrite, generally lacking significant internal structure and often ovoid in shape. Many, but not all, pellets are of fecal origin.

Sparse allochems sufficiently scarce so as to be separated from each other by carbonate mud; less than 50% of the rock (Folk, 1959, 1962).

Pelmicrite a limestone composed dominantly of peloids (or pellets) in a matrix of micrite (Folk, 1959, 1962).

Spastolith refers to an ooid which has been deformed by shearing the concentric laminations away from the nucleus.

Peloid an allochem formed of cryptocrystalline or microcrystalline carbonate irrespective of size or origin. This term allows reference to grains composed of micrite or microspar without the need to imply any particular mode of origin (can thus include pellets, some vague intraclasts, micritized fossils, ooids, etc.).

Stylolite a jagged, columnar surface in carbonate rocks which may be at any orientation relative to bedding; often associated with large amounts of insoluble material, and produced by solution and grain interpenetration. Sucrose carbonate rocks that have appreciable intercrystal pore space and are composed dominantly of somewhat equant, uniformly sized, euhedral to subhedral crystals.

Pelsparite a limestone composed dominantly of peloids (or pellets) in sparry calcite cement (Folk, 1959, 1962). Penecontemporaneous generally referring to cements or replacement textures indicating that, in the opinion of the user, the feature or mineral formed at almost the same time as the original sediment was deposited, that is, close to the sediment-air or sediment-water interface. Phreatic the zone of water saturation below the water table. There are marine or meteoric phreatic zones.

Syntaxial refers to overgrowths which are in optical continuity with their underlying grains. Telogenetic occurring during the time interval during which long buried sediments or rocks are influenced significantly by processes associated with the formation of an unconformity.

Pisolite a small spheroidal particle with concentrically laminated internal structure and size larger than 2 mm.

Terrigenous derived from the land area and transported mechanically to the basin of deposition; commonly, essentially synonymous with "noncarbonate" (e.g. terrigenous sand vs. carbonate sand).

Poikilotopic (poikilitic) textural term denoting a condition in which small granular crystals are irregularly scattered without common orientation in a larger crystal of another mineral (generally sand or silt grains in a single cement crystal).

Tufa (calctufa) a sedimentary rock (limestone or silica) deposited in or around springs, lakes and rivers from emerging ground waters charged with CO2 and CaCC^ or SiC^- Commonly builds thick calcite deposits rich in algae and higher plant material.

Poorly Washed a rock which has sparry calcite cement but which also has one-third to one-half of all interstices filled with carbonate mud (i.e., a poorly sorted rock).

Umbrella Void a void (perhaps later filled with sparry calcite) produced by the presence of a large grain sheltering the underlying area by preventing infiltration of mud-sized grains. Also called shelter porosity.

Primary Porosity porosity present in the rock or sediment immediately after final deposition.

Vadose designates the area above the water table (zone of aeration) in which both water and air are present in pores.

Pseudospar a neomorphic (recrystallization) calcite fabric with average crystal size larger than 30 microns (Folk, 1965). Radiaxial Fabric a cavity-filling spar mosaic consisting of fibrous crystals radiating away from the wall, allied to optic axes which converge away from the wall. Also characterized by curved cleavages and irregular intergranular boundaries.

VIII

Vug a pore that is somewhat equant, is larger than 1/16 mm in diameter, and does not specifically conform in position, shape or boundary to particular fabric elements to the host rock (i.e., is not fabric selective). Generally formed by solution. Wackestone carbonate rock composed of carbonate mud with over 10% allochems suspended in it (Dunham, 1962).

Grain Size Scales for Sediments ,-

The grade scale most commonly used for sediments is the Wentworth scale (actually first proposed by Uddenl, which is a logarithmic scale in that each grade limit is twice as large as the next smaller grade limit. For more detailed work, sieves have been constructed at intervals

U.S. Standard Sieve Mesh #

Millimeters

The <j> (phi) scale, devised by Krumbein, is a much more convenient way of presenting data than if the values are expressed in millimeters, and is used almost entirely in recent work.

Microns (iMTli

4096 1024 256

Use

and 4 /-_- .

Phi (<j>)

Wentworth Size Class

-12 -10

Boulder (-8 to-120) Cobble (-6 to -80)

64 16 4 3.36 2.83 2.38

- 4 2 - 1.75 - 1.5 - 1.25

12 14 16

1.68 1.41 1.19

- 0.75 - 0.5 - 0.25

20 25 30 35 40 45 50 60 70 80 100 —120 140 170 200

0.84 0.71 0.59 420 350 300 250 210 177 149

0.25 0.5 0.75 1.0 1.25 1.5 1.75 2.0 2.25 2.5 2.75

105 88 74

3.25 3.5 3.75

Very fine sand

4.25 4.5 4.75

Coarse silt

wire squares 5 6 7 8

270 325

Analyzed

bv Pipette or Hydrometer

II

0.42 0.35 0.30 1/4 — 0.25 0.210 0.177 0.149 1/8 — 0.125 0.105 0.088 0.074 0.053 0.044 0.037 1/32 — 0.031 1/64 0.0156 1/128 0.0078 1/T56 0 0039 0.0020 0.00098 0.00049 0.00024 0.00012 0.00006

1 111

- 6

53 44 37 31 15.6 7.8 39 2.0 0.98 0.49 0.24 0.12 0.06

6.0 7.0 8 0 9.0 10.0 11.0 12.0 13.0 14.0

Pebble (-2 to -60)

Granule

<

o

Very coarse sand

Coarse sand

Q Medium sand

Z <

Fine sand

Medium silt Fine silt Very fine silt Clay

(From Folk, 1968)

IX

>

U)

Q

2

Grain Scales: cont. Comparison Chart For Visual Percentage Estimation (After Terry and Chilingar, 1955).

X

SKELETAL COMPOSITIONS TAXON

CALCITE

ARAG.

%Mg

CALCAREOUS ALGAE: RED GREEN

0

5

1

i

10 15 20 25 3 0 35 i

i

i

I

V

I

BOTH ARAGO AND CAL

I

V

X

COCCOLITHS FORAMINIFERA:

X

BENTHONIC

V .1 A

0

... "•

V A

"

-V "A

x-x

PLANKTONIC SPONGES:

X

0

X

COELENTERATES: STROMATOPORIDS (A)

X

MILLEPOROIDS

X

X?

x...

RUGOSE (A) TABULATE (A)

x?

SCLERACTINIAN ALCYONARIAN

X V A

0 0

BRYOZOANS: BRACHIOPODS: MOLLUSKS: CHITONS PELECYPODS GASTROPODS

X X X

PTEROPODS CEPHALOPODS (MOST)

v A

X X X-X

0

x-x x-x

X X

X X

BELEMNOIDS & APTYCHI (A)

X

ANNELIDS (SERPULIDS):

X

v A

V A

X

ARTHROPODS: DECAPODS

X—X

OSTRACODES

X

BARNACLES

X—X

TRILOBITES (A)

X

ECHINODERMS: X Common

X 0 Rare

X

X

(A) Not based on modern forms

XI

by the Geological Society of America offers good summaries of fossil groupings, skeletal structure, and mineralogy. Most volumes have now been published and they contain extensive references. Only a few other references will therefore be included here. Biggild, 0 . B., 1930, Shell structure of molluscs: K. Danske Vidensk. Selskabs Skrifter, 9 Raekke, Natur og Math. Afd. 2, p. 231-321. Very detailed shell structure and mineralogy of recent and fossil mollusks. Quite accurate despite lack of X-ray data. Bonet, Federico, 1956, Zonificacion microfaunistica de las calizas Cretacicas del este de Mexico: Asoc. Mexicana Geologos Petroleros Bol., v. 8, p. 389-488. Details of calcisphere, calpionellid, and foraminiferal zonation of the Cretaceous. Flugel, Erik, ed., 1977, Fossil Algae; recent results and developments: New York, Springer-Verlag, 375 p. Hay, W. W., K. M. Towe, and R. C. Wright, 1963, Ultramicrostructure of some selected foraminiferal tests: Micropaleontology, v. 9, p. 171-195. Johnson, J. H., 1961, Limestone-building algae and algal limestones: Golden, Colorado, Colorado School Mines, 297 p. .4 well-illustrated introduction. Johnson also has several other books on specific algal groups of individual geologic periods also published as Colorado School of Mines Quarterlies. Sorauf, J. E., 1971, Microstructure in the exoskeleton of some Rugosa (Coelenterata): Jour. Paleontology, v. 45, p. 23-32. Sorauf, J. E., 1972, Skeletal microstructure and microarchitecture in Scleractinia (Coelenterata): Palaeontology, v. 15, p. 88-107. Tavener-Smith, R., and A. Williams, 1972, The secretion and structure of the skeleton of living and fossil Bryozoa: Royal Soc. London Philos. Trans., ser. B, v. 264 (859), p. 97-159. Taylor, J. D., W. J. Kennedy, and A. Hall, 1969, The shell structure and mineralogy of the Bivalvia: Introduction, Nuculacea-Trigonacea: British Mus. (Nat. Hist.) Bull., Zoology, Suppl. 3, 125 p. Includes light microscopy and SEM. Wise, S. W., Jr., 1970, Microarchitecture and mode of formation of nacre (mother-of-pearl) in pelecypods, gastropods, and cephalopods: Eclogae Geol. Helvetiae, v. 63, p. 775-797. Wray, J. L., 1977, Calcareous algae: New York, Elsevier, 185 p. A good summary of taxonomic and stratigraphic information; includes photomicrographs and some SEM's.

Selected Bibliography

Fossil and Grain Identification: General Bathurst, R. G. C , 1971, Carbonate sediments and their diagenesis: New York, Elsevier, 620 p. Although this is a general text, it offers about 75 pages of discussion, and some good thin-section and SEM photos of skeletal grains. Carozzi, A. V,, and D. A. Textoris, 1967, Paleozoic carbonate microfacies of the eastern stable interior (U.S.A.): Leiden, E. J. Brill, 146 p. Illustrates assemblages of grains in numerous microfacies. Cita, M. B., 1965, Jurassic, Cretaceous and Tertiary microfacies from the southern Alps: Leiden, E. J. Brill, 99 p. Good photos of Mesozoic and Cenozoic fossil and grain assemblages with special emphasis on deeper-water facies. Cuvillier, J., 1961, Stratigraphic correlation by microfacies in western Aquitaine: Leiden, E. J. Brill, 34 p. Photos of Jurassic to Tertiary microfaunal and macrofaunal assemblages. Hay, W. W., S. W. Wise, Jr., and R. D. Stieglitz, 1970, Scanning electron microscope study of fine grain size biogenic carbonate particles: Gulf Coast Assoc. Geol. Socs. Trans., v. 20, p. 287-302. Provides some guideline for the identification of the source of very finely comminuted skeletal debris. Horowitz, A. S., and P. E. Potter, 1971, Introductory petrography of fossils: New York, Springer-Verlag, 302 p. General but good quality photos of fossils, grains, and microfacies assemblages. Johnson, J. H., 1951, An introduction to the study of organic limestones: Colorado School Mines Quart., v. 46, no. 2, 185 p. A very general introduction with good photos of macro- and microfossil groups. Inexpensive. Majewske, 0 . P., 1969, Recognition of invertebrate fossil fragments in rocks and thin sections: Leiden, E. J. Brill, 101 p. (plus 106 plates). Detailed, excellent photos and determinative tables for identification of shells from structural details. Expensive. Milliman, J. D., 1974, Marine carbonates: New York, Springer-Verlag, 375 p. A general text with some photos of whole and thin sectioned organisms; gives excellent summaries of geochemical data for each group. Moore, R. C , C. G. Lalicker, and A. G. Fischer, 1952, Invertebrate fossils: New York, McGraw-Hill, 766 p. General text with good illustrations of internal structures of various fossil groups. Tasch, Paul, 1973, Paleobiology of the invertebrates: New York, John Wiley and Sons, 946 p. A general paleontology text. Wilson, J. L., 1975, Carbonate facies in geologic history: New York, Springer-Verlag, 471 p. Discusses the regional distribution of carbonate facies through time; includes 30 plates of important microfacies textures.

Carbonate Classification Dunham, R. J., 1962, Classification of carbonate rocks according to depositional texture, in W. E. Ham, ed., Classification of carbonate rocks: AAPG Memoir 1, p. 108-121. Folk, R. L., 1962, Spectral subdivision of limestone types, in W. E. Ham, ed.. Classification of carbonate rocks: AAPG Memoir 1, p. 62-84. Other classifications, less frequently used, are also found in this volume.

Carbonate Cements Bathurst, R. G. C , 1971, Carbonate sediments and their diagenesis: New York, Elsevier, 620 p. A well-written synthesis of what is known and what isn 't known abou t carbonate cements. Bricker, 0 . P., ed., 1971, Carbonate cements: Baltimore, Johns Hopkins Press, 376 p. Contains a wide range of articles on cement textures and compositions from marine and nonmarine environments. Folk, R. L., 1974, The natural history of crystalline calcium carbonate; effect of magnesium content and salinity: Jour. Sed. Petrology, v. 44, p. 40-53. Presents data on role of water chemistry of carbonate cement morphologies. James, N. P., R. IM. Ginsburg, D. S. Marszalek, and P. W. Choquette, 1976, Facies and fabric specificity of early subsea cements in shallow Belize (British Honduras) reefs: Jour. Sed. Petrology, v. 46, p. 523-544.

Fossil Identification: Specific Groups Treatise on Invertebrate Paleontology. This series of books published

XII

Meyers, W. J., 1974, Carbonate cement stratigraphy of the Lake Valley Formation (Mississippian) Sacramento mountains. New Mexico: Jour. Sed. Petrology, v. 44, p. 837-861.

Lane, D. W., 1962, Improved acetate peel technique: Jour. Sed. Petrology, v. 32, p. 870. Lindholm, R. C , and R. B. Finkelman, 1972, Calcite staining: semiquantitative determination of ferrous iron: Jour. Sed. Petrology, v. 42, p. 239-242. McCrone, A. W., 1963, Quick preparation of peel-prints for sedimentary petrography: Jour. Sed. Petrology, v. 33, p. 228-230. McDougall, D. J., ed., 1968, Thermoluminescence of geological materials: London, Academic Press, 675 p. Medlin, W. L., 1959, Thermoluminescent properties of calcite: Jour. Chem. Physics, v. 30, p. 451-458. Ostrom, M. E., 1961, Separating clay minerals from carbonate rocks by using acid: Jour. Sed. Petrology, v. 3 1 , p. 123-129. Royse, C. F., Jr., J. S. Wadell, and L. E. Peterson, 1971, X-ray determination of calcite-dolomite; an evaluation: Jour. Sed. Petrology, v. 4 1 , p. 483-488. Runnells, D. D., 1970, Errors in X-ray analysis of carbonates due to solid-solution variation in composition of component minerals: Jour. Sed. Petrology, v. 40, p. 1158-1166. Schneidermann, Nahum, and P. A. Sandberg, 1971, Calcite-aragonite differentiation by selective staining and scanning electron microscopy: Gulf Coast Assoc. Geol. Socs. Trans., v. 2 1 , p. 349-352. Siesser, W. G., and John Rogers, 1971, An investigation of the suitability of four methods used in routine carbonate analysis of marine sediments: Deep-Sea Research, v. 18, p. 135-139. Smith, M. H., 1970, Identification of organic matter in thin section by staining and a study program for carbonate rocks: Jour. Sed. Petrology, v. 40, p. 1350-1351. Weber, J. N., 1968, Quantitative mineralogical analysis of carbonate sediments; comparison of X-ray diffraction and electron probe microanalyser methods: Jour. Sed. Petrology, v. 38, p. 232-234. Wolf, K. H., A. J. Easton, and S. Wame, 1967, Techniques of examining and analyzing carbonate skeletons, minerals, and rocks, in G. V. Chilingar, H. J. Bissell, and R. W. Fairbridge, eds.. Carbonate rocks: New York, Elsevier, Devel. in Sedimentol. 9B, p. 253-341.

Carbonate Recrystallization Bathurst, Ft. G. C , 1971, Carbonate sediments and their diagenesis: New York, Elsevier, 620 p. Presents a number of alternative points of view on questions of cementation versus recrystallization. Folk, R. L., 1965, Some aspects of recrystallization in ancient limestones, in l_. C. Pray, and R. C. Murray, eds., Dolomitization and limestone diagenesis, a symposium: SEPM Spec. Publ. 13, p. 14-48. An excellent introduction to the basic concepts. Folk, R. L., 1973, Carbonate petrography in the post-Sorbian age, in R. N. Ginsburg, ed., Evolving concepts in sedimentology: Baltimore, Johns Hopkins Univ. Press, p. 118-158. A general summary of precipitation and recrystallization. Purdy, E. G., 1968, Carbonate diagenesis; an environmental survey: Geol. Romana, v. 7, p. 183-228. Sandberg, P. A., 1975, Bryozoan diagenesis; bearing on the nature of the original skeleton of rugose corals: Jour. Paleontology, v. 49, p. 587-606. Discusses evidence for inversion of aragonite to calcite based on light microscopy and SEM.

Porosity Classification Choquette, P. W., and L. C. Pray, 1970, Geologic nomenclature and classification of porosity in sedimentary carbonates: AAPG Bull., v. 54, p. 207-250. By far the best article available on this subject. This paper and other useful articles on the subject are contained in AAPG Reprint Series No. 5, Carbonate rocks I I : Porosity and classification of reservoir rocks.

Techniques References Cited Dickson, J. A. D., 1966, Carbonate identification and genesis as revealed by staining: Jour. Sed. Petrology, v. 36, p. 491-505. Diebold, F. E., J. Lemish, and C. L. Hiltrop, 1963, Determination of calcite, dolomite, quartz, and clay content of carbonate rocks: Jour. Sed. Petrology, v. 33, p. 124-139. Ellingboe, John, and James Wilson, 1964, A quantitative separation of non-carbonate minerals from carbonate minerals: Jour. Sed. Petrology, v. 34, p. 412-418. Evamy, 8. D., 1963, The application of a chemical staining technique to a study of dedolomitization: Sedimentology, v. 2, p. 164-170. Fischer, A. G., S. Honjo, and R. W. Garrison, 1967, Electron micrographs of limestones and their nannofossils: Princeton, Princeton Univ. Press, Monographs in Geol. and Paleont. No. 1, 141 p. Flugel, Erik, H. E. Franz, and W. F. Ott, 1968, Review on electron microscope studies of limestones, in G. Miiller, and G. M. Friedman, eds., Recent developments in carbonate sedimentology in central Europe: New York, Springer-Verlag, p. 85-97. Folk, R. L., 1968, Petrology of sedimentary rocks: Austin, Texas, Hemphill's, 170 p. Friedman, G. M., 1959, Identification of carbonate minerals by staining methods: Jour. Sed. Petrology, v. 29, p. 87-97. Goldsmith, J. R., D. L. Graf, and H. C. Heard, 1961, Lattice constants of the calcium-magnesium carbonates: A m . Mineralogist, v. 46, p, 453-457. Goldstein, J. I., and Harvey Yakowitz, eds., 1975, Practical scanning electron microscopy; electron and microprobe analysis: New York, Plenum Press, 582 p. Katz, A., and G. M. Friedman, 1965, The preparation of stained acetate peels for the study of carbonate rocks: Jour. Sed. Petrology, v. 35, p. 248-249.

Choquette, P. W., and L. C. Pray, 1970, Geologic nomenclature and classification of porosity in sedimentary carbonates: AAPG Bull., v. 54, p. 207-250. Dunham, R. J., 1962, Classification of carbonate rocks according to depositional texture, in W. E. Ham, ed., Classification of carbonate rocks: AAPG Memoir 1, p. 108-121. Folk, R. L., 1962, Spectral subdivision of limestone types, in W. E. Ham, ed., Classification of carbonate rocks: AAPG Memoir 1 , p. 6284. 1965, Some aspects of recrystallization in ancient limestones, in L. C. Pray and R. C. Murray, eds., Dolomitization and limestone diagenesis, a symposium: SEPM Spec. Pub. 13, p. 14-48. 1968, Petrology of sedimentary rocks: Austin, Texas, Hemphill's, 170 p. 1974, The natural history of crystalline calcium carbonate; effect of magnesium content and salinity: Jour. Sed. Petrology, v. 44, p. 40-53. Scholle, P. A., 1971a, Sedimentology of fine-grained deep-water carbonate turbidites, Monte Antola Flysch (Upper Cretaceous), northern Apennines, Italy: Geol. Soc. America Bull., v. 82, p. 629-658. 1971b, Diagenesis of deep water carbonate turbidites. Upper Cretaceous, Monte Antola Flysch, northern Apennines, Italy: Jour. Sed. Petrology, v. 4 1 , p. 233-250. and D. J. J. Kinsman, 1974, Aragonitic and high-Mg calcite caliche from the Persian Gulf—a modern analog of the Permian of Texas and New Mexico: Jour. Sed. Petrology, v. 44, p. 904-916. Terry, R. D., and G. V. Chilingar, 1955, Summary of "Concerning some additional aids in studying sedimentary formations," by M. S. Shvetsov: Jour. Sed. Petrology, v. 25, p. 229-234.

XIII

Skeletal Grains Algae

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3 Holocene algae B i o l o g i c a l preparation ( w i t h stain) of Anabaena heterocysts. Rather typical of spherical blue-green algal bodies which link up into chains. Such algae, in combination with filamentous forms, are common in modern algal mats.

0.022 mm

Holocene

algae

B i o l o g i c a l preparation ( w i t h stain) of Rivularia heterocysts. These are filamentous blue-green a l g a e . The individual c e l l s can be seen stained purple and the m u c i l a g i nous sheaths are stained green. Such interlocking filaments help trap p a r t i c l e s in blue-green algal mats through a baffling effect as well as slight stickiness.

0.027 mm

T r i a s s i c Dachstein L s . , Lofer focies Austria A very w e l l developed ancient example of a laminated and contorted blue-green algal mat ( l o f e r i t e ) . Dark reddish-brown color, s l i g h t l y pelletal texture, and irregular lamination are c h a r a c t e r i s t i c of blue-green algal mats but are not always this clearly displayed.

0.64 mm

Up. Silurian part of TonolowayKeyser Ls« Pennsylvania Blue-green algal stromatolite (biolithite) showing moderate lamination, pelleting, and fenestrae. Even where algal lamination is very clear in outcrop it may be quite subtle in thin section.

0.38 mm

Mid. Ordovician Bays L s . equivalent Virginia Burrowed blue-green algal stromatolite (biolithite) showing vague lamination, characteristic pelleting and large spar-filled vugs possibly related to burrowing or syndepositional gas generation.

0.38 mm

Up. Permian Capitan Fm, New Mexico Blue-green algae can also produce irregular encrustation of grains, as in this sponge reef. Several large, poorly preserved sponges are seen with dark, lumpy coatings (some " f l o a t i n g " in sparry calcite). These are often considered to be algal although some would interpret them as cement rinds.

0.64 mm

5 Up. Permian Capitan Fm. New Mexico These m u l t i p l e , laminated c r u s t s surround many grains in the Permian reef complex of New Mexico and appear to have played a major r o l e in the l i t h i f i c a t i o n of the reef d e b r i s . It is presumed that these crusts are the result of blue-green a l g a l g r o w t h .

0.19 mm

Up. Devonian Jean Marie Fm. Canada (N.W.T.) The dark m i c r i t i c , lumpy patches are Renalcis, an important bluegreen a l g a l type w h i c h , in the Devonian of Canada, is restricted to the reef and very near-reef f a c i e s . It thus i s an important tool in the recognition of nearby reefs.

X.N.

0.22 mm

U p . Devonian Jean Marie Canada (N.W.T.)

Fm.

Another view of Renalcis structure i l l u s t r a t i n g the commonly scalloped o u t l i n e of these blue-green algae, as w e l l as their m i c r i t i c t e x t u r e .

0.25 mm

6

Eocene Green River Fm. Wyoming A head of Chlorellopsis coloniata, a probable blue-green algal stromatolite builder. Although the stromatolite is largely replaced by chert, one can still see laminated structure with circular, calcisphere-like bodies. These heads are common in lacustrine facies.

0.64 mm

Mid. Cambrian Meagher L s . Montana Closeup of an algal nodule (oncolite) showing very small, irregular tubules characteristic of the possible blue-green alga Girvanella. These tubes are often well preserved but can only be seen with close observation and relatively high magnification.

0.05 mm

Up. Permian Capitan Ls. New Mexico Section of a Tubiphytes colony characterized by very dense, dark micritic material with broadly spaced darker banding. This is an encrustation on reef material and has been assigned by some workers to the algae and by others to the hydrozoans.

0.64 mm

7 Holocene bottom quez Key) Florida

sediment

(Rodri-

Cross s e c t i o n of a Holocene C o d i acian green alga (llalimeda sp.) showing the dark c a l c i f i e d plate w i t h abundant irregular holes o r i g i n a l l y f i l l e d w i t h organic matter. T h i s is one of the major carbonate sand producers in modern reefs.

0.30 mm

Holocene al gae Florida Closeup of the structure green alga Halimeda showing regular tubes and c a l c i f i e d plate. Dark blebs are air images.

of the the irmain bubble

0.38 mm

P l e i s t o c e n e Key L a r g o L s . Florida Altered grain of Halimeciu (green alga) showing t y p i c a l preservation of t h i s type of grain. O r i g i n a l holes are f i l l e d w i t h spar and most of the plate has also altered to spar. Structure shown only by m i c r i t e " e n v e l o p e s " surrounding o r i g i n a l h o l e s .

X.N.

0.24 mm

Holocene sediment Florida Cross s e c t i o n of a Halimeda plate showing tubular opening, o r i g i n a l l y o c c u p i e d by plant t i s s u e , and c a l c i f i e d areas w i t h abundant, i n t e r l o c k e d , rather randomly oriented aragonite needles w h i c h make up the preservable portion of the Halimeda plate.

SEM Mag. 1000X

Holocene Florida

13 fim

sediment

Close-up of Halimeda plate showing details of i n t e r l o c k i n g aragonite needles. Needles such as these are found in many species of green algae i n c l u d i n g Penicillus, Udotea, and others* When the algae decompose, the needles may be scattered and add s i g n i f i c a n t l y to the local production of c l a y - s i z e d particles (carbonate mud).

SEM Mag. 10,000X

Oligocene Florida

1.3 Mm

Suwannee

Ls.

A d a s y c l a d green alga showing t y p i c a l l y poor p r e s e r v a t i o n . Most of the l i g h t l y c a l c i f i e d plate structure has been destroyed and o n l y traces of the o r i g i n a l structure remain.

0.38 mm

Up. Cretaceous Colombia

limestone

Large green-algal (Dasycladacean) grain w i t h oblique cut through central c a v i t y and r a d i a t i n g porous tubes. Presence of tubes is major feature a l l o w i n g i d e n t i f i c a t i o n as a green algal fragment.

X.N.

Cretaceous Mexico

0.25

Tamabra

Ls.

Cross section d i r e c t l y across o Dasycladacean green a l g a . Shows radial symmetry of elements about the central c a v i t y . The characteri s t i c features w h i c h a l l o w i d e n t i f i cation are the presence of r a d i a t i n g tubes and a central c a v i t y coupled w i t h poor preservation of w a l l s t r u c ture.

0.64

Up. Permian Capitan Fm. t r a n s i t i o n New Mexico

Ls.-Tansill

Abundant Mizzia, a type of Dasycladacean green algae very abundant in near-back-reef facies of the P e r m i a n . C h a r a c t e r i s t i c radial symmetry, tubular structures, poor w a l l preservation, and central c a v i t y are shown in a number of the grains. The green color is stained p l a s t i c in voids*

0.64 mm

10 M i d - P e n n s y l vanian Paradox Fm.

Utah P h y l l o i d algal grain showing relat i v e l y good p r e s e r v a t i o n . Note parall e l , short t u b u l e s w h i c h l i n e the outer margins o f the g r a i n . These are q u i t e c h a r a c t e r i s t i c when well preserved but must be d i s t i n g u i s h e d from m i c r i t e envelopes or grain coating m i c r i t e . These grains are very important in Penn syl vanian bioherms.

0.22

P e n n s y l v a n i u n I s . , Sacramento Mtn s., New Mexi co Another r e l a t i v e l y w e l l preserved p h y l l o i d algal grain showing marginal tubules, some of w h i c h have c o l l a p s e d into the grain i n t e r i o r during d i s s o l u t i o n . Very poor preservat i o n of a l l portions except the mudf i l l e d tubes is quite t y p i c a l .

0.25

Mi d-Pennsyl vanian Minturn F m . Colorado Poorly preserved phylloid algal plates ( p o s s i b l y of green algae). A l l internal structure has been o b l i t erated and o n l y structural o u t l i n e s remain.

0.38

11 M i d - P e n n s y l v a n i a n Minturn Fm. Colorado T y p i c a l l y poor preservation of probable green ( p h y l l o i d ) a l g a e . Note complete replacement by sparry c a l c i t e with no preservation of internal structure.

0.38 mm

L o . Cretaceous Newark Canyon F m . Nevada Oblique sections through the veget a t i v e parts of two charophytes., These plants are c l a s s e d as green algae; modern as w e l l as a n c i e n t forms appear to be r e s t r i c t e d to nonmarine ( e s p e c i a l l y l a c u s t r i n e ) environments. Charophytes can be major rock-forming elements as w e l l as important b i o s t r a t i g r a p h i c markers i n nonmarine sediments.

0.30 mm

L o . Cretaceous Newark Canyon Fm. Nevada Transverse section through the veget a t i v e part of a charophyte. Shows c h a r a c t e r i s t i c central tube w i t h surrounding c o r t i c a l t u b e s . C a l c i f i e d gyrogonites (oogonia) often occur in a s s o c i a t i o n w i t h the v e g e t a t i v e remains.

0.30

12 Holocene bottom guez Key) Florida

sediment

(Rodri-

Fragment of Goniolithon red-algal grain. Note characteristic fine cellular structure. Although red-algal grains i n v a r i a b l y are converted from o r i g i n a l high-Mg to eventual low-Mg c a l c i t e during diagenesis, the f i n e scale c e l l u l a r structure is normally preserved.

0.30 mm

M i d . Eocene Coamo Springs L s . Puerto Rico l.ithophyllum red-algal grain showing c e l l u l a r and laminated structure as w e l l as spore cases (small round w h i t e spots).

0.24 mm

Tertiary calcarenite Muscat and Oman Very well preserved red alga, p o s s i bly Litbuphyllum. T h i s example shows d i f f e r e n t i a t i o n of central hypothallus and the denser, external perithallus. The c e l l u l a r structure, branching form, and good preservation distinguish these coralline algae from other algal types.

0.38

13 Upo Eocene limestone Germany

fi?J%

An e n c r u s t i n g red a l g a , p o s s i b l y Lithoporella melobesioides. Shows regular c e l l u l a r structure w i t h irregular e n c r u s t i n g strips and concepta c l e chambers. Red-algal encrusta t i o n s are very important in modern reef development as they provide much of the b i n d i n g of grains into a wave-resistant framework

0.22 mm

Mid v Eocene Coamo Springs Ls~ Puerto Ri co L a r g e red-algal fragment with typical laminated and c e l l u l a r structures. C u t by numerous d o l o m i t e rhombs (often s e l e c t i v e l y replacing red algae because of o r i g i n a l high Mg content).

0.38

Cretaceous Mexico

Tamabru

Ls.

A large algal grain from a r u d i s t i d bioherm. T h i s c o u l d be a C o d i acean green alga or p o s s i b l y a red algao Note abundant mud-filled tubes. Where mud has not i n f i l l e d tubes r e c r y s t a l l i z a t i o n would have e f f e c t i v e l y o b l i t e r a t e d this g r a i n .

0.64 mm

14 Cretaceous Tamabra Ls» Mexico A probable Solenoporoid grain w i t h i n a r u d i s t i d reef. Note r a d i a t i n g tubes w i t h c e l l u l a r s t r u c t u r e . In many areas, t h i s structure is largely obliterated by r e c r y s t a l l i z a r i o n . in t h i s group, the cross p a r t i t i o n s sepa r a t i n g c e l l s are w e a k l y c a l c i f i e d and often do not preserve w e l l , y i e l d i n g a tubular structure rather than a c e l l u l a r one.

0.64 mm

Cretaceous Tamabra L s . Mexico Several types of encrusting algae. The large tubular form may be a red a l g a , whereas the dark, m i c r i t i c , lumpy forms are probably blue-green a l g a e . T h i s i l l u s t r a t e s the complex intergrowth of a l g a l types and their importance in h o l d i n g together reef material (such as these r u d i s t i d fragments).

0.64 mm

15

Miscellaneous Microfossils

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17 Eocene deep water ooze, DSDP leg 1 Bermuda R i s e , N . A t l a n t i c Ocean Abundant c o c c o l i t h s (smear mount) showing c h a r a c t e r i s t i c curved-cross extinction pattern. R e c o g n i t i o n of c o c c o l i t h s in normal-thickness t h i n sections is much more d i f f i c u l t and can only be accomplished along u n u s u a l l y thin edges of the s l i d e . C o c c o l i t h s , members of the goldenbrown algae, range from J u r a s s i c to Holocene.

X.N.

0.016

M i d . Miocene, DSDP Leg 12 Site 116 H a t t o n - R o c k a l l B a s i n , N. A t l a n t i c Ocean SEM view of a c o c c o l i t h ooze. Sediment is composed almost entirely of c o c c o l i t h plates and fragments with subordinate di scoasters and fragments of planktonic Foraminifera. V i r t u a l l y no cement; sediment s t i l l has about 60 percent porosity. Some corrosion of c o c c o l i t h s is evident, a common syn- and post-depositional feature in deep sea sediments.

SEM Mag. 5000X

2.5Mm

Up. Cretaceous A t c o Fm. of A u s t i n Group Texas An example of an exposed, onshore chalk. Some well-preserved coccol i t h s are v i s i b l e along with numerous c o c c o l i t h fragments, clay minerals, spines, and other skeletal fragments. This chalk was probably deposited in no more than 200 meters of water and s t i l l retains about 25-30 percent porosity.

SEM Mag. 3000X

4.3 jam

18 U p . Cretaceous A t c o Fm. of A u s t i n

Group Texas SEM view of a single c o c c o l i t h from the chalk in the previous photo. It is w e l l preserved w i t h v i r t u a l l y no d i s s o l u t i o n or cementation a f f e c t i n g its outline.

SEM Mag. 14.500X

0.9 ft m

Holocene plankton B e l i z e ( B r i t i s h Honduras) A coccosphere of Emiliania huxleyi, Coccospheres are the o r i g i n a l , undisaggregated h o l l o w spheres formed by interlocking coccolith plates* T h e y are found o c c a s i o n a l l y in undisturbed chalk sediments,, although most t e n d to f a l l apart into constituent p l a t e s .

SEM Mag. 10,OOOX

1.3

pm

Holocene plankton B e l i z e ( B r i t i s h Honduras) A partly broken coccosphere of Emiliania huxleyi showing the f a c t that each c o c c o l i t h is r e a l l y a double plate and that adjacent c o c c o l i t h s i n t e r l o c k in a tongueand-groove manner to form a c o c c o sphere.

SEM Mag. 10,000X

1.3 jam

19 M a e s t r i c h t i a n chalk Denmark SEM view of a rhabdol i t h . T h i s is a coccoli th-type plate with a long spine attached to the outer surface. It is quite common to find the rhabd o l i t h spines broken off; such spines can often compose a s i g n i f i c a n t portion of c h a l k s .

SEM Mag. 6000X

2.2 Mm

Pliocene? marine sediment P a c i f i c Ocean A discoaster in SEM v i e w . These star-shaped nannofossils are espec i a l l y important in Cenozoic s t r a t i graphic z o n a t i o n .

SEM Mag. ca. 10,000X

1.3 nm

Up. J u r a s s i c C a l p i o n e l l i d L s .

Italy A single U-shaped c a l p i o n e l l i d . V i s i ble only at r e l a t i v e l y high m a g n i f i c a t i o n , these m i c r o f o s s i l s are quite important in J u r a s s i c and Cretaceous deep-water sediment and are useful in the stratigraphic zonation of those deposits.

0.014 mm

Up. Jurassic Calpionellid L s . Italy

Section through a single c a l p i o n e l l i d showing c l a s s i c vase or urn shape. A large v a r i e t y of shapes are known but many incorporate t h e feature of a straight or curved l i p around the aperture, as seen here.

0.014 mm

U p . Pennsyl vanian Mbr., Graham F m . Texas

Gunsight

Ls.

Walled c a l c i s p h e r e s (of possible green algal origin) a s s o c i a t e d w i t h m i c r i t i z e d and spar f i l l e d s k e l e t a l d e b r i s . In Devonian to Permian carbonates c a l c i s p h e r e s are e s p e c i a l l y important in r e s t r i c t e d or back reef environments.

0.38 mm

U p . Cretaceous (Cenomanian) L o w e r Chalk England A c a l c i sphere limestone. The bulk o f the m i c r o f o s s i l s in t h i s s e c t i o n are c a l c i s p h e r e s of the genera Oligostegina and Pitbonella. T h e y show a w e l l - d e f i n e d w a l l w h i c h is d i f f i c u l t to d i s t i n g u i s h from single chambers of some p l a n k t o n i c Foraminifera. Pithonella ovalis can show a very e l l i p t i c a l o u t l i n e w i t h a large apert u r e . These grains are very common in Cretaceous p e l a g i c d e p o s i t s .

0.11 mm

21 Up. Cretaceous C h a l k North Sea A chalk w i t h abundant c a l c i s p h e r e s , p o s s i b l y Pithonella ovalis. Note the s i n g l e , spherical chambers and the d i s t i n c t i v e w a l l texture of these grains as w e l l as the s m a l l , assoc i a t e d c o c c o l i t h s in the background.

S E M M a g . 1000X

12.5 fim

Up Cretaceous Buda L s . Texas U n w a l l e d calcispheres in a m i c r i t e matrix. These calcispheres may be of non-algal o r i g i n ( e . g . a l t e r a t i o n of radiolarians).

0.10

Holocene

sediment

B e l i z e ( B r i t i s h Honduras) V i e w s of a s i n g l e t u n i c a t e s p i c u l e , T u n i c a t e s are c l a s s e d in the subphyllum Hemichordata, and some genera have c a l c i t i c s p i c u l e s embedded in their f l e s h y t i s s u e . They make up as much as 1 percent of the sediment in some modern settings in shallow water. They are charact e r i z e d by their multi-rayed shape and very small s i z e .

X.N.

0.016 mm

22

U p . Cretaceous New Jersey

Red Bank Sand

Stained preparation of a d i n o f l a g e l l a t e Deflandria diebeli. Central portion (endocyst) and spinose appendages (horns) have stained d i f f e r entially. D i n o f l a g e l lates can be useful in correlation of marine sediments of T r i a s s i c to Recent age.

0.027 mm

Up. Cretaceous Mount L a u r e l Sand New Jersey A stained preparation of the dinof l a g e l late Spiniferites ramosus. -rhe central portion has taken a dark s t a i n and the m u l t i p l e , r a d i a t i n g , s p l a y - t i p p e d or trumpet-like appendages are c l e a r l y v i s i b l e . These resting c y s t s are n o n c a l c i f i e d .

0.022 mm

Cretaceous(?) sediment

SEM view of a single dinoflagel late, probably Oligosphaeridium sp. The central portion of the body and the r a d i a t i n g s appendages w i t h their t r i angular terminations are shown.

SEM Mag. ca. 1000X

12.5 M m

23

Paleozoic(?) sediment U n i t e d States SEM v i e w of a herkomorph a c r i t a r c h . T h i s is a f o s s i l group of uncertain taxonomic a f f i n i t y , l i k e l y produced by zooplankton as w e l l as phyto= plankton. They range from Precambrian t o Holocene and are commonly found in p a l y n o l o g i c a l preparations ( H C I - H F residue).

SEM Mag. c a . 800X

17 Mm

Paleozoic(?) sediment U n i t e d States SEM v i e w of another a c r i t a r c h of t o t a l l y different form of the group Polygonomorphitae. A n a l g a l a f f i n i t y has been suggested for t h i s group. Acritarchs, like dinoflagellates, are n o n - c a l c i f i e d but may frequently be found in calcareous r o c k s , esp e c i a l l y in p a l y n o l o g i c a l preparations.

SEM Mag. ca. 800X

17 fim

J u r a s s i c ( T i t h o n i a n ) P o i n t Sal o p h i o l i t e group California Longitudinal cross s e c t i o n of a single radiolarian text. Originally o p a l , t h i s example has gone to quartz chert and s t i l l shows the coarse pore structure in the outer s k e l e t o n . T h i s group is wide ranging and extremely important in formation of deep-water d e p o s i t s e s p e c i a l l y in the D e v o n i a n , J u r a s s i c , and Tertiaryb

0.07 mm

24

Jurassic (Tithonian) Point Sol ophiolite group California Cross sections through two radiolaria showing good preservation of tests despite alteration from opal to chert. Coarse pore structure,, size, and shape of tests are main criteria for identification.

0.07 mm

Up. Jurassic{?) radiolarite Muscat and Oman Tangential section through the poorly preserved outer wall of a radiolarian. In the alteration of opal tests to cristobalite and, finally, to quartz, much of the structural detail may be lost. But coarse pore structure is still visible.

0.03 mm

Up. Jurassic(?) radiolarite Muscat and Oman Section through a poorly preserved radiolarian test. Some traces of coarse, radial pore structure or outer wall is still visible.

0.03 mm

25 Up. J u r a s s i c part of F r a n c i s c a n Fm. California

•r/V

SEM view of a s i n g l e radiolarian w h i c h has been etched out of a chert w i t h H F a c i d . The radiolarian is also composed of chert but etches out s e l e c t i v e l y . Note coarse pore structure and shape.

•

;:

• '^<*M

§•****

#.v#

;»?££#: >

•

«

%

• ' • * • •

•

mi Mf>;•£M

SEM Mag. ca. 300X

.mm . . .:-..,,

, ,.

.

41 jlim

Holocene sediment Mexico An o p a l i n e diatom t e s t . Diatoms are important in Cretaceous and T e r t i a r y sediments from a number of environments. O r i g i n a l l y composed of o p a l , they alter to other forms of s i l i c a , often w i t h very considerable loss of textural d e t a i l . Note small bit of a broken sponge s p i c u l e w h i c h overlaps d i a t o m .

\

V

0.018 mm

Holocene sediment B e l i z e ( B r i t i s h Honduras) SEM view of numerous marine d i a toms on a sponge s p i c u l e . Although most are o v a l - s h a p e d , one elongate diatom can be seen in the lower left. Diatoms (and their d e p o s i t s — d i a t o mites) can be found in both marine and fresh-water s e t t i n g s , often in close association with carbonate sediments, p a r t i c u l a r l y in the M i o cene of the c i r c u m - P a c i f i c area.

SEM Mag. 3000X

4.6

m

26 Miocene Monterey Shale Cal ifornia A s i l i c e o u s shale which can be seen to c o n s i s t almost e x c l u s i v e l y of fragmented marine diatoms. These are s t i l l o p a l ; conversion to c r i s t o b a l i t e or quartz-chert normally i n volves the loss of much of the textural detai I seen here.

SEM Mag. 6000X

2 yum

Holocene sediment, Shagawa L a k e Minnesota Four specimens of Stepbanodiscus sp., a nonmarine diatom from a eutrophic freshwater lake. Diatoms, a group of s i l i c e o u s algae, are known from sediments at least as old as J u r a s s i c and can be useful in paleoecologic as well as biostratigraphic interpretations.

S E M M a g . 4750X

2,5 yum

L o . Missi ssippian Cottonwood Canyon Mbr. of Lodgepole L s . Montana Abundant conodonts, mainly from the genus Sipbonodella. These minute t o o t h - l i k e or p l a t e - l i k e f o s s i l s are of uncertain b i o l o g i c a l a f f i n i t y but are extremely important in Paleozoic b i o s t r a t i g r a p h i c zonation. A l though rarely found in t h i s abundance, they are common in carbonate rocks. The color of conodonts in transmitted l i g h t has been used as an index of the degree of thermal a l t e r a t i o n of the sediments.

0.38 mm

27

L o . M i s s i s s i p p i a n Cottonwood Canyon Mbr. of L o d g e p o l e L s . Montana Several l o n g i t u d i n a l and transverse s e c t i o n s of conodonts (mainly Siphonodella sp.) are v i s i b l e . Note characteristic plates with pronounced denticles. Section a l s o c o n t a i n s abundant quartz sand and some darkbrown f i s h d e b r i s .

0.38 mm

L o . Mi s s i s s i p p i a n C o t t o n w o o d C a n yon Mbr. of L o d g e p o l e L s . Montana Same v i e w as above but under c r o s s polarized light. Illustrates typical extinction behavior of conodonts with pronounced appearance of " w h i t e m a t t e r " w i t h i n saw-toothed extinction pattern.

X.N.

0.38 mm

29

Foraminifera

This page intentionally left blank.

31 Up. Eocene Ocala L s . Florida Miliolid Foraminifera with largely m i c r i t i z e d and pores w i t h chalcedonic chert.

X.N.

walls filled

0.24

:

'.wwm,~$m Up. Eocene Ocala L s . (Ingiis) Florida M i l i o l i d Foraminifera w i t h largely o b l i t e r a t e d wall structure and part i a l l y cemented p o r o s i t y .

X.N.

0.24

L o . Cretaceous Cupido Fm. Mexico A limestone composed largely of m i l i o l i d Foraminifera. These are e s p e c i a l l y common in s l i g h t l y res t r i c t e d back-reef or bank f a c i e s . T h i s example shows some of the variety of shapes which can result from random s l i c e s through m i l i o lids.

0.22 mm

32 Holocene sediment B e l i z e ( B r i t i s h Honduras)

Peneroplid Foraminifera showing c h a r a c t e r i s t i c shape, structure and shell color (for Holocene specimens only).

0.24

H o l o c e n e sediment B e l i z e (British* Honduras) Peneroplid Foraminifera showing t y p i c a l shapes and structures, and i l l u s t r a t i n g early diagenetic changes within depositional environmentsome a l t e r a t i o n of w a l l texture has taken p l a c e and much of the intragranular p o r o s i t y has been l o s t .

X.N.

0.24 mm

L o . Permian Bone Spring L s . Texas F u s u l i n i d Foraminifera in section a c r o s s long a x i s . Note chamber shapes and radial w a l l structure. Very common in P e n n s y l v a n i a n and Permian sediments.

0.38 mm

33 Eocene Nummulite I s . Jugoslavia

L o n g - a x i a l section of a s i n g l e Foraminifera, Nummulites sp. These large Foraminifera can be major rock forming elements in Eocene s e d i ments.

X.N.

0.38 mm

M i d . Eocene Coamo Springs L s . Puerto Rico L o n g - a x i a l section of a single raminifera, Discocyclina sp.

Fo-

0.38 mm

Up. Cretaceous Del Rio Clay Texas Arenaceous Foraminifera showing chambers composed of agglutinated i n d i v i d u a l q u a r t z - s i l t grains.

X.N.

0.38

34

Up. Cretaceous Lower C h a l k England Section through a s i n g l e a g g l u t i n a t i n g Foraminifera—in t h i s case one w h i c h selects both carbonate and non-carbonate g r a i n s . These Foraminifera are r e c o g n i z a b l e by the chamber-shaped grain arrangements rather than the o t h e r w i s e random arrangement of grains in the rest of the rock.

0.10 mm

M i d . P e n n s y l v a n i a n Paradox Fm. Utah Sections through u n i s e r i a l und b i serial F o r a m i n i f e r a . Note micrit i z e d w a l l structures and t y p i c a l chamber shapes^

X.N.

0.25 mm

Cretaceous (Cenomanian) Is. Austria Section through a s i n g l e , large Orbit o l i n i d F o r a m i n i f e r a . These Forami n i f e r a can be important rock formers in Cretaceous sediments.

0.37 mm

35 L o . and M i d . Pennsylvanian Fm. Oklahoma

Bloyd

Encrusting Foraminifera on a neomorphosed pelecypod s h e l l . Globular, chambered foraminiferal structure is vaguely v i s i b l e w i t h i n the dense, m i c r i t i c areas. Encrusting foraminifera are commonly misinterpreted as encrusting algae.

X.N. •-

0.22

•*>

Holocene coral-rubble beach B e l i z e ( B r i t i s h Honduras

ridge

Cross section of a large e n c r u s t i n g Foraminifera--WOffzo/remtf rubrurn w i t h very regular w a l l and c e l l s t r u c t u r e . Reddish t i n t i s c h a r a c t e r i s t i c of t h i s species.

0.38

Up. Cretaceous Upper C h a l k

England

A Gtobotruncana sp. planktonic F o r a m i n i f e r a . Q u i t e common in Cretaceous sediments, t h i s example shows the very poor w a l l preservation that i s frequently found. Note the k e e l e d chambers.

0.04 mm

36 Holocene ooze, 1000 meter depth, Coral Sea, P a c i f i c Ocean A modern p e l a g i c ooze f i l l e d w i t h Globorotalia. Globorotalids and g l o b i g e r i n i d s have spherical chamb e r s , r a d i a l l y porous w a l l structures and commonly very t h i c k w a l l s . They are an extremely important component of the p l a n k t o n i c assemblage in L a t e Cretaceous and T e r t i a r y deeper water sediments.

0.17 mm

Pleistocene(?) ooze Offshore F l o r i d a (Miami Terrace) G l o b o r o t a l i d Foraminifera showing w e l l - p r e s e r v e d porous radial w a l l structure and m i c r i t e f i l l i n g of chambers. These organisms are plankt o n i c and normally are most abundant in outer shelf to oceanic s e d i ments.

X.N.

0.10 mm

U p . Cretaceous Greenhorn L s . Colorado Thin-walled globigerinid Foraminifera w i t h s p a r - f i l l e d chambers.

X.N.

0.06 mm

37 Holocene sediment B e l i z e ( B r i t i s h Honduras)

SEM view of a single specimen of Sagrina (Bolivina) pulchella. It shows b i s e r i a l chambers, pores in w a l l s and external ornamentation.

SEM Mag. 300X 43 Mm

Holocene sediment B e l i z e ( B r i t i s h Honduras) SEM view of a s i n g l e specimen of Rectobolivina adrena. This uniserial Foraminifera shows porous wall and attached spines.

SEM Mag. 300X

43 y-m

Holocene sediment B e l i z e ( B r i t i s h Honduras) SEM view of a s i n g l e specimen of Globigerinoides rubra, a planktonic Foraminifera. Globular chambers, small spines and pores in w a l l , as well as large aperature, are c l e a r l y

visible.

SEM Mag. 150X 86 pm

38 Holocene sediment B e l i z e ( B r i t i s h Honduras) SEM v i e w of a s i n g l e specimen of Pyrgo sp. Shows smooth, non-perforate w a l l and globular chambers. N e x t photo shows detail of test surface t e x t u r e .

SEM Mag. 150X

86nm

Holocene sediment B e l i z e ( B r i t i s h Honduras) SEM closeup of Pyrgo sp. Note t i g h t l y packed, oriented laths of c a l c i t e which make up w a l l . With degradation of the organic b i n d i n g mat e r i a l , or g r i n d i n g of the shell by natural processes, these laths could c o n t r i b u t e to the production of carbonate mud.

SEM Mag. 10.000X

1.3 Mm

Holocene sediment B e l i z e ( B r i t i s h Honduras) SEM closeup of Spiroloculina sp. View is of a fractured w a l l showing inner and outer shell surfaces, as w e l l as a cross section of the w a l l itself* Note the bladed c r y s t a l s w h i c h make up the w a l l and their changing o r i e n t a t i o n toward the shell surface.

SEM Mag. 10,000X

1.3/xm

Annelids and Related Groups

This page intentionally left blank.

41 L o . Cretaceous Glen Rose L s . Texas L a r g e serpulid worm tubes b u i l t of concentric laminae of c a l c i t e , and often a d j o i n i n g and o v e r l a p p i n g . Elongate, spar-filled voids parallel to laminar w a l l structure are chara c t e r i s t i c of s e r p u l i d s .

0.38 mm

Cretaceous Glen Rose L s . Texas Detail of large serpulid worm tube; shows j u n c t i o n of two tubes and micrite f i l l i n g of tubes. Note coarse, s l i g h t l y irregular, concentric lamination.

0.38 mm

Jurassic beds England

C o r a l l i a n Series,

Trigonia

Serpulid worm tubes can be seen encrusting on an altered Trigonia (pelecypod) s h e l l . The s m a l l , y e l l o w to w h i t e patches w i t h i n the serpulid shell w a l l s are areas of s11icification .

1.] 8 mm

42 Holocene sediment Florida Sabelariid worm tubes encrusting mangrove roots (not seen). These tubes are agglutinated and are v i s i ble only as o r i e n t e d , imbricated grains which surround c i r c u l a r pore space. Green t i n t i s stained i m p r e g nating medium.

1.10 mm

Holocene Florida

sediment

Closeup of a s i n g l e Sabelariid tube showing the n o n s e l e c t i v e use of several types of grains, their orientation w i t h long axes tangential to tube o u t l i n e , and the very sparse binding m a t e r i a l . Green-stained areas are f i l l e d w i t h stained impregn a t i n g medium.

0.34 mm

Up. Devonian Genundewa L s . New York Abundant examples of Stylolina fissurella. These are s m a l l , c o n i c a l f o s s i l s which are c l a s s e d as conul a r i i d s and placed with the A n n e l i d s and other worms by some p a l e o n t o l ogists. S t y l o l i n a and other s i m i l a r forms are important rock-formers and index f o s s i l s at some levels in the Paleozoic.

0.11

w U ft 10, • &« mgtgm u « « & *

43 Devonian Germany

Tentaculiten

Knottenkalk

A cut through a t e n t a c u i i t e p a r a l l e l to the long a x i s . Shows c o n i c a l shape and crenulate or corrugate exterior. These are s i m i l a r to StyloUna except for the external ornament a t i o n , and are classed by some as belonging to the worms; others place them w i t h the m o l l u s k s .

0.11 mm

Devonian Germany

Tentaculiten

Knottenkalk

Several o b l i q u e cuts through Tentaculites sp. showing the pronounced corrugation of the s h e l l . A l s o note w a v y , laminated shell structure.

0.11 mm

45

Archaeocyathids and Sponges

This page intentionally left blank.

47 Cambrian A j a x L s . Australia Cross section of an A r c h a e o c y a t h i d wall. Central c a v i t y is at the top with double w a l l in center and external sediment at bottom. The inner and outer w a l l s confine a series of radial compartments. These organisms may be related to sponges ( a l though they are commonly placed in a separate phyllum), were r e s t r i c t e d to the Cambrian, and b u i l t reefs or bioherms in many areas.

0.64 mm

Cambrian A j a x Australia

Ls.

Cross section of an A r c h a e o c y a t h i d w a l l w i t h central c a v i t y in upper right. Shows radial compartments formed by double w a l l structure w i t h septate p a r t i t i o n s .

0.25 mm

Up. Permian Capitan L s . New Mexico A large calcareous sponge w i t h enc r u s t i n g blue-green a l g a e . A s w i t h most sponges, s k e l e t a l preservation is poor but vague o u t l i n e s of chambers can be seen. These sponges were major contributors to the Permian reef complexes of New Mexico and T e x a s .

1.24 mm

48

L o . Permian Getaway L s . Mbr. of Cherry Canyon Fm. Texas Large, originally calcareous sponge which shows large cavities preserved as voids or with sediment i n f i l l . Sponge wall structure has been obliterated by si licification. Irregular chamber shapes and large size aid in identification.

0.64 mm

Up. Pennsylvanian Graford Fm. Texas A rather well preserved sponge— Maeandrostia sp. (a calei sponge). Note central cavity and irregular lateral chambers. Although little of the original wall structure is preserved, the original outlines of wall positions are clearly marked by changes in color due to inclusions in neomorphic calcite.

0.64 mm

Lo. Ordovician Group Texas

part

of

El

Paso

A part of a large calcareous sponge showing irregular canals filled with micrite. Original wall structure has been completely obliterated through dissolution and reprecipitation of sparry calciteo The vague, meandering structural pattern is typical of many sponges.

0.64 mm

49 Lo< Cretaceous Lower Green sand England A cross section of a small portion of the calcareous sponge Raphidonema jarringdonense. Note meandering canal structure and w e l l - p r e s e r v e d w a l l structure. Canals are partly f i l l e d w i t h hematite.

0.38 mm

Holocene reef sediment Jamaica L o n g i t u d i n a l section of a modern sclerosponge (Ceratoporella sp.(?)). T h i s organism contributes greatly to the deeper-water parts of modern Caribbean reefs. Skeleton is aragon i t e arranged in conical bundles. These organisms have been grouped w i t h the sponges, coelenterates, or stromatoporoids.

G.P.

Holocene Jamaica

$ 3 8 mm

reef

sediment

Transverse section of the same specimen as above. Note c i r c u l a r o u t l i n e s of aragonitic fiber bundles in this s e c t i o n .

0.38 mm

50 Silurian Brownsport Gp. Tennessee I n t e r l o c k i n g six-rayed (in this plane) s p i c u l e s of the sponge Astraeospongia meniscus. Each s p i c u l e is a s i n g l e c a l c i t e c r y s t a l w i t h u n i t ext i n c t i o n ; i n t e r l o c k i n g spokes make up the skeletal framework of the sponge.

0.64 mm

L o . and M i d . Pennsylvanian Marble Falls L s . Texas Sponge s p i c u l e s in a clayey matrix. M o s t of these spicules are monaxons and show characteristic central canal and s p i c u l e shape. A l l were o r i g i n a l l y o p a l i n e s i l i c a ; now some are chert, some c a l c i t e . Not a l l sponge spicules have a central c a n a l , however.

0.24 mm

L o . and Mid. Pennsylvanian Marble Falls Ls. Texas Sponge s p i c u l e s . Shows same area as previous p i c t u r e but under polarized l i g h t . Chert and c a l c i t e replacements of spicules are v i s i b l e .

X.N.

0.24 mm

Up- Jurassic or Radiolarite Muscat and Oman

Lo.

Cretaceous

Cross sections of Monaxon sponge spicules. One is a transverse section across a spicule, the other parallel to trie long axis of a spicule. Note the thick walls and central canal characteristic of many originally opaline spicules.

0.04 mm

Up- Cretaceous White Limestone Northern Ireland A spicule-rich sediment showing outlines of sponge spicules (which are now found as voids). Note the mixture of monaxons and multiaxoned spicules. The grains with central fillings are calcispheres and planktonic Foraminifera.

0.25 mm

Holocene sediment Belize (British Honduras) SEM view of a modern siliceous sponge showing smooth, interlocked, diversely oriented opaline spicules. Upon death of the sponge, these spicules can be widely dispersed and loose spicules are commonly found in modern sediments from shallow-water and deep-water environments.

S E M M a g . 300X

43 fim

53

Stromatoporoids

This page intentionally left blank.

55 Up. Devonian Is. Iowa An Actinostroma sp.(?) stromatoporoid showing the general undul a t i n g , head-shaped c o l o n i a l farm with pore structures p a r a l l e l i n g the exterior of the colony as w e l l as pores w h i c h run perpendicular to the exterior. T h i s y i e l d s a very crude and irregular box-work structure seen in more detail in the n e x t photograph.

1.18 mm

Up- Devonian I s . Iowa An Actinostroma sp.{?) stromaroporoid showing sheeted structure with regular and irregular open spaces. T h i s colony has a headshaped form. Stromatoporoids are major rock forming elements in many Upper P a l e o z o i c limestones and contributed e x t e n s i v e l y to the framework formation of reefs and bioherms.

« r •/<

f t

•»• - i $.'••• i

>*3

0.38

' i

Up. Silurian C o b l e s k i l l L s . New York A stromatoporoid (Stromatopora constellata) showing layered boxwork structure plus ovoid-to-round sparf i l l e d holes. Preservation average to s l i g h t l y better than average.

1.18

56 Cretaceous El Abra Fm. Mexico A probable sphaeractinid (e.g. Parkeria) or other stromatoporoidrelated hydrozoan. They occur as spherical, marble-to-golf-ball-sized nodules in the near-back-reef facies. A coarse pore structure and a tubular wall texture are visible.

0.64 mm

jr

* X ,>*

57

Corals

This page intentionally left blank.

59

Holocene back-reef beach sand Belize (British Honduras) Relatively unaltered (but rounded) Scleractinian coral fragment illustrating high initial intragranular porosity. Note irregular coral lite shapes in this section.

X.N.

0.38

Pleistocene back-reef Is. Belize (British Honduras) Closeup of a segment of a large Scleractinian coral showing original septa (central dark line with surrounding trabecular structure) and partial filling of living chambers. Considerable recrystallization has occurred even in samples as young as Pleistocene.

X.N.

0.38 mm

Pleistocene Key Largo Ls. Florida Segment of a large Scleractinian coral head showing growth lines with trabecular (fibrous bundle) structure and complete filling of intragranular porosity by carbonate cement.

X.N.

0.24 mm

60 Paleocene (Danian) F a k s e L s . Denmark Oblique s e c t i o n through the Sclera c t i n i a n coral Dendrophyllia candelabra showing radial arrangement of septa. Wall structure ent i r e l y o b l i t e r a t e d during i n v e r s i o n from aragonite to c a l c i t e . Recogn i z a b l e on the basis of the shape of internal chambers and septa as w e l l as their s i z e .

0.64

A.

Holocene sediment B e l i z e ( B r i t i s h Honduras) SEM v i e w of a broken section of Montastrea annularis. The trabecular structure w i t h c r y s t a l s radia t i n g out from points can be seen. T h i s grain is e n t i r e l y aragonitic and has seen v i r t u a l l y no a l t e r a t i o n .

SEM Mag. 800X

16fxm

Holocene sediment B e l i z e ( B r i t i s h Honduras) SEM view of the margin of chamber of Montastrea annularis showing the early diagenetic cementation of the porosity of c o r a l s . L o n g needles of aragonite are seen growing into the chamber w h i l e algal(?) tubes add another small component. Such early cementation may a l l o w preservation of some of the w a l l structure during later d i a g e n e s i s .

SEM Mag. 1000X

13jum

.

s

i •

Hi

61 H o l o c e n e sediment B e l i z e ( B r i t i s h Honduras) SEM v i e w of broken portion of the s c l e r a c t i n i a n coral Agaricia agaricides. One can see bundles of bladed c r y s t a l s w h i c h make up the trabecular w a l l s t r u c t u r e .

1,,,:, SEM Mag. 3000X %

4.3 »m

*

Holocene Florida

sediment

The clear and purple structures are s p i c u l e s w h i c h normally are embedded in the t i s s u e of Gorgonians (Alcyonaria). T h i s is a clorox r e s i due of a s i n g l e coral colony and shows the types of s p i c u l e s w h i c h may be released to the sediment upon decay of the organic matter of Gorgonians.

0.24 mm

M i d . Pennsylvanian Paradox Fm. Utah A completely silicified tabulate c o r a l . In t h i s section one does not see the tabulae. Only the e l l i p t i c a l to c i r c u l a r tubes w h i c h are growing c l o s e l y - s p a c e d and parallel to one another are seen.

0.64

62

Up. P e n n s y l v a n i a n Graham Fm. Texas Cross section of a s o l i t a r y rugose coral Lophophyllidium proliferum. The s i m p l e , r a d i a t i n g septa and c e n tral (or a x i a l ) complex are w e l l preserved and show o u t l i n e s of o r i g i n a l septal texture w i t h trabecular structure. A l l these features, as well as the large size of the c o r a l l i t e s , help to d i f f e r e n t i a t e coral and bryozoan fragments.

0.64 mm

Up. Devonian is. Iowa A portion of a large c o l o n i a l rugose cora\--Pachyphyllum woodmani. T h i s example shows moderate preservation of r a d i a t i n g septa and the axial complex. The Rugosa are e s p e c i a l l y important as reef and bioherm builders in Devonian to Pennsylvanian time.

1.24 mm

Up. Devonian i s . Iowa Section of the c o l o n i a l coral Pacby phyllum woodmani showing differential preservation of main septal w a l l s and c r o s s w a l l s .

X.N.

0.38

W-S^^m^^i: %

63 L o . Carboniferous Coral L s . England Large s o l i t a r y rugose coral in oblique cut. See subsequent photos for more d e t a i l e d v i e w s of w a l l structure. L a r g e c o r a l l i t e s , radia t i n g septa and d i s s e p i m e n t s , vari a t i o n s in c o r a l l i t e shape and differences in t h i c k n e s s of various types o f w a l l s are used to d i s tinguish corals from s u p e r f i c i a l l y similar bryozoans.

1.24 mm

L o . Carboniferous Coral L s . England Closeup of large s o l i t a r y coral. Has t h i n , dark growth lines of o r i g i n a l dissepiments plus spar f i l l i n g s of chambers. Note thicker w a l l in upper right-hand corner; t h i s i s chara c t e r i s t i c of coral skeletons.

X.N.

0.38 mm

L o . Carboniferous Coral L s . England Closeup of large solitary coral showing irregular chamber shapes and dissepiments of varying t h i c k n e s s . Sparry c a l c i t e f i l l s chambers.

X.N.

0.38 mm

65

Bryozoans

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67 Up. Permian Capitan L s . New Mexico L a r g e bryozoan frond w i t h regular c i r c u l a r to elongate holes (zooecia) and f i n e l y fibrous w a l l structure.

0.38 mm

Up. Silurian Keyser L s . Pennsylvania

part

of

Tonoloway-

Cross section of a bryozoan stem showing f a i r l y regular rounded chambers and t h i c k , fibrous w a l l structure.

0.10

Up- Silurian Keyser L s . Pennsylvania

part

of

Tonoloway-

Section of long a x i s of a s t i c k shaped bryozoan w i t h c h a r a c t e r i s t i c i n c l i n e d c e l l u l a r structure and regular, fibrous w a l l s .

X.N.

0.38 mm

68

Up. Pennsylvanian Canyon Gp. Texas

Winchell

Ls.

of

Cross section of a fenestrate bryozoan w i t h t y p i c a l skeletal structure (note e s p e c i a l l y the thick fibrous wails).

P.X.N.

0.30 mm

Up. P e n n s y l v a n i a n Winchell L s . of

Canyon Gp. Texas Fenestrate bryozoan cut in a section showing separation of individual segments.

0.38 mm

M i s s i s s i p p i a n biohermal mound Kansas Fenestrate bryozoan in a spar matrix. Shows l i t t l e structure except for the i c h a r a c t e r i s t i c even spacing of i s o l a t e d segments. T h i s is a common texture in M i s s i s s i p p i a n reefs.

0.38 mm

69 Mi s s i s s i p p i a n flank) L s . Ireland

Waulsortian

(reef-

Abundant circular and elongate fenestrate bryozoans compose entire rock fabric. Shows the large amount of pore space (now f i l l e d w i t h sparry c a l c i t e cement) which can be present in loosely packed bryozoan sediments.

1.24 mm

Up. Permian Bell Canyon Fm. Texas L a r g e bryozoan fragment in reef t a l u s . Shows unusually good preservation of zooecia because of early, f i n e l y c r y s t a l l i n e d o l o m i t i zation. Z o o e c i a tend to be smaller and more uniform than c o r a l l i t e s .

0.64

Up- Permian B e l i Canyon Fm. Texas A different cut through the same specimen as above. Note the chara c t e r i s t i c shape of the zooecia and their curvature toward the margins of the colony.

0.64 mm

70

Up. P e n n s y l v a n i a n Graham Fm. Texas A series of three s e c t i o n s through a cryptostome bryozoan, Megacantbopora sp. This transverse cross section through the stick-shaped colony shows the radial d i s t r i b u t i o n o f zooecia and the t h i c k e n e d w a l l structure at the exterior margins.

0.64 mm

U p . P e n n s y l v a n i a n Graham Fm. : Texas A l o n g i t u d i n a l section through the same specimen as above. Shows curvature of zooecia toward outer margins and again i l l u s t r a t e s the t h i c k ening of w a l l structure toward the exterior.

0.64 mm

Up- P e n n s y l v a n i a n Graham Fm. Texas An o b l i q u e section through the same specimen as above. Shows uniform to slightly e l l i p t i c a l zooecia and fibrous calcitic wall structure. T h e s e 3 photos i l l u s t r a t e the range o f d i f f e r e n t structures which are poss i b l e in a s i n g l e specimen given various a n g l e s of s e c t i o n i n g .

0.64 mm

V •

71 UpSilurian Keyser L s . Pennsylvania

part

of

Tonoloway-

L a r g e bryozoan frond showing t y p i cal shape and structure.

0.30

Pleistocene Key Largo L s . Florida Section of a s i n g l e colony of the modern encrusting bryozoan Scbizo* pore Ha floridana. The central area, now p a r t l y f i l l e d w i t h i n f i l t r a t e d sediment, once h e l d the encrusted organism (probably some T h a l a s s i a grass). These encrusters are most abundant today in the somewhat res t r i c t e d bay and lagoonal environments.

1.24

M i d . and U p . O r d o v i c i a n Martinsburg Fm. Virginia A large bryozoan colony with irregular z o o e c i a l shapes but characteri s t i c outward rotation of zooecia at margins.

0.10 mm

73

Brachiopods

This page intentionally left blank.

75

M i d . Ordovician Black River L s . Pennsylvania Several elongate brachiopod s h e l l s (plus other grains) showing crenulate shape of many brachiopod shells.

X.N.

0.38 mm

M i d . Ordovician Black River L s . Pennsylvania Large brachiopod shell w i t h wavy, parallel laminated shell structure sub-parallel to shell edge.

0.38

Up. Silurian Keyser L s . Pennsylvania

part

of

T onoloway-

Brachiopod shell with parallel fibrous structure running sub-para l l e l ( i n c l i n e d about 15 degrees) to the outer margin of s h e l l . Shell is a simple one or two layered structure, u n l i k e most mollusk s h e l l s .

X.N.

0.38 mm

76 Up. M i s s i s s i p p i a n H i n d s v i l l e L s . Oklahoma Shows a number of coated brachiopod grains (as w e l l as c r i n o i d p l a t e s ) . A l l the brachiopods have low-angle fibrous wall structure. One c l e a r l y shows the a d d i t i o n a l outer w a l l (with perpendicular arrangements of f i bers). Another shell shows m i c r i f e f i l l e d punctate structure, and a t h i r d shows impunctate structure with wavy shell contortion.

0.25 mm

Up- M i s s i s s i p p i a n H i n d s v i l l e L s . Oklahoma A punctate brachiopod. Has clearly defined pores or punctae which comp l e t e l y penetrate the shell and here are f i l l e d w i t h m i c r i t i c sediment. Sediment also contains micrite coated echinoderm and bryozoan fragments.

0.25

Up. Ordovician R e e d s v i l l e Shale Pennsylvania Brachiopod shell w i t h parallel f i brous structure. A l s o shows some oblique pseudopunctae.

X.N.

0.30 mm

77

L o . Devonian Becraft L s . New York

Section through a pseudopuncfate brachiopod s h e l l . Note the parallel fibrous w a l l structure w i t h small plications which run vertically through the s h e l l . These are the pseudopunctae; they do not represent actual openings or pores in the shelL

0.11

Up.

Permian

Capitan

Ls.

(reef

facies) New Mexico Section of a portion of the w a l l of Composita sp=, a brachiopod w i t h an atypical prismatic wall structure. T h i s particular group of brachiopods is r e s t r i c t e d to Carboniferous and Permian sediments. These s h e l l s can be d i f f e r e n t i a t e d from p e l e c ypods on the basis of the presence of internal calcareous spires in the Composita (not a l w a y s preserved).

X.N.

0.51 mm

M i s s i s s i p p i a n Glencar L s . Ireland Three brachiopod spines w i t h concentric parallel fibrous inner, and r a d i a l - f i b r o u s outer w a l l layers, as w e l l as hollow central c a n a l .

0.09 mm

78 L o . Permian Bone Spring L s . Texas T r a n s v e r s e cross-section of a brachiopod spine. Note fibrous structure yielding pseudo-uniaxial cross, central c a n a l , and outer w a l l .

X.N.

0.08 mm

Mississippian G l e n c a r L s . Ireland Oblique l o n g i t u d i n a l cross section of a brachiopod spine. L a y e r e d , fibrous w a l l structure is c h a r a c t e r i s t i c of such grains.

0.09 mm

79

Mollusks

This page intentionally left blank.

81 Holocene sediment B i m i n i , Bahamas

An example of crossed-lamellar w a l l s t r u c t u r e - o n e of the major types of a r a g o n i t i c textures in m o l l u s k s . T h i s example i s from a gastropod. Note the narrow bands of a l t e r n a t i n g l i g h t and dark e x t i n c t i o n w h i c h wedge out along a x i s .

X.N.

0.09 mm

Holocene sediment B e l i z e ( B r i t i s h Honduras)

J** •V' ~:r

4

M,

•^::.:::.;i:,::N::'

SEM v i e w of a broken shell of Pecten (Lyropecten) sp. Shell w a l l shows i n t e r s e c t i n g bundles of aragonite crystals characteristic of crossed-lamellar structure.

SEM Mag. 1000X

12.5

/tm

::

Up. O l i g o c e n e M o l a s s e Germany Part of a large Cyrenia shell e a s i l y r e c o g n i z a b l e as a mollusk by i t s shell shape. Has homogeneous structure w i t h e x t i n c t i o n bands perp e n d i c u l a r to outer shell w a l l (and sweeping the length of the shell as stage i s rotated).

*'**" $4 1

X.N.

0.38 mm

82 Up. Cretaceous San Carlos Fm. Texas

An Inoceramus shell w i t h very d i s t i n c t i v e p r i s m a t i c structure. Often these s h e l l s break up into i n d i v i d u a l prisms w h i c h may c o n s t i t u t e an important fraction of some sediments. Note boring in shell w a l l .

X.N.

0.38 mm

Up. Cretaceous Upper Chalk England Micritic sediment with numerous, scattered, individual inoceramus prisms. The large variation in shape i s due to d i f f e r e n t angles of cut through p r i s m s , but all are recogn i z a b l e by their s i z e , shape, and c h a r a c t e r i s t i c e x t i n c t i o n behavior.

X.N.

0.30 mm

H o l o c e n e sediment B e l i z e ( B r i t i s h Honduras) SEM v i e w of a broken shell of Pinna sp. Note the large prisms w h i c h are arranged perpendicular to the margin of the shell and w h i c h c o n s t i t u t e the e n t i r e shell w a l l . Most organisms w i t h p r i s m a t i c - s t r u c t u r e d shell w a l l s secrete p r i m a r i l y c a l c i t e .

SEM Mag. 100X

125

Mm

83 P l i o c e n e and P l e i s t o c e n e Caloosahatchee Marl Florida Cross section of an oyster shell showing a l t e r n a t i n g constructional layers of lamellar and v e s i c u l a r c a l c i t e . V e s i c u l a r structure is common in ostreid m o l l u s k s .

X.N.

.

0.38 mm

': ' f T S M U r

Holocene sediment B e l i z e ( B r i t i s h Honduras)

Holocene sediment B e l i z e ( B r i t i s h Honduras)

SEM view of broken mollusk s h e l l . The nacreous layer (shown here) cons i s t s of s t a c k e d , overlapping vertical column s of tabular aragonite c r y s t a l s separated by thin sheaths of organic material.

SEM closeup of the nacreous layer of a mollusk shell showing detail of the i n t e r l o c k i n g aragonite t a b l e t s . Although t h i s structure is lost during d i a g e n e s i s , i t is useful in i d e n t i f i cation of modern shell fragments.

S E M M a g . 2000X

SEM Mag. 10,000X

6.2 a m

I.J p,m

84 Pliocene and Pleistocene Caloosahatchee Marl Florida Bored fragment of an oyster shell. Borings (dark patches) are filled with lime mud (micrite), and shell shows multilayered structure (alternating horizontal-foliated and vertical crossed-lamellar structure).

X.N.

0.38 mm

Up- Cretaceous Rio Yauco Fm. Puerto Rico •Jf

Fragment of a rudistid mollusk. Rudistids have complicated and variable shapes but are often recognizable by the boxwork (vesicular) structure of their shells.

X.N.

4,

0.38 mm

Up. Cretaceous (Santonian) Kroner Reef L s . Germany A large fragment of the Chamacean pelecypod Hippurites sp. (a close relative of other rudistids). Again recognizable by the vesicular boxwork texture. Distinguished from corals, bryozoans, etc. by the size, shape, and details of vesicular structure.

0.64 mm

: 

*£* *?> ^>r^

':*.

85 Cretaceous Tamabra Ls. Mexico

Section of the wall of o probable radiolitid rodist illustrating the well preserved cellular prismatic outer layer of the shell. These rudists are major contributors to Cretaceous reefs and bioherms.

0.64 mm

Cretaceous Tamabra Ls. Mexico

**«tf % - .

Section of the wall of a probable caprinid rudist showing canals within the very poorly preserved (once, presumably, aragonitic) shell wall. These rudists were also important reef and bioherm builders in the Cretaceous. Micritic encrustation visible in upper part of photograph is probably algal.

0.64 mm

Cretaceous El Abra Ls. Mexico Section through a small portion of the wall of a toucasiaid rudist (Diceratidae) shows two distinct shell layers. One (exterior) retains original structure and pigmentation; the other is completely recrystallized to calcite and is marked by line of "perched" miliolid Foraminifera.

0.64 mm

86 Triassic Germany

(Karnian)

Hallstatter

Ls.

Numerous t h i n - w a l l e d s h e l l s of the P e c t i n o i d pelecypod, Halobia sp. These very t h i n s h e l l s were adapted to a p o s s i b l y m o t i l e e x i s t e n c e on soft bottoms or may even have been p e l a g i c , and are common in T r i a s s i c deeper-water sediments. Recognizable by shape.

0.64 mm

L o . and M i d . P e n n s y l v a n i a n B l o y d Fm. Oklahoma A foram-encrusted, partly r e c r y s t a l l i z e d pelecypod with very large external shell p l i c a t i o n s . T h i s grain i s c l e a r l y r e c o g n i z a b l e as molluscan on the b a s i s of shape alone.

X.N.

0.22 mm

L o . Cretaceous Cupido Fm. Mexico Two pelecypods showing common mode of a l t e r a t i o n . These were o r i g i nally aragonitic shells which i n verted to c a l c i t e by a d i s s o l u t i o n p r e c i p i t a t i o n mechanism. T h i s o b l i t erated a l l r e l i c t internal shell structure. Grains are i d e n t i f i a b l e only on the basis of c h a r a c t e r i s t i c shapes o u t l i n e d by m i c r i t e envelopes.

0.22 mm

87

Lo. Cretaceous Glen Rose Ls. Texas

These are the internal fillings of pelecypods--Corbula sp. All trace of the shell wall is gone and the only way to distinguish these complex pelletal grains from intraclasts is by their consistent "tear-drop" shape. The shells were rolled during the infiltration of sediment, yielding complex fillings.

0.64

Up. Miocene Hydrobien Ls. Germany A well-sorted gastropod limestone composed entirely of the freshwater meso-gastropod prosobranchs, Hydrobia sp. Note the variety of shapes produced by different angles of section through these gastropods. Shells are aragonitic and have crossed-lamelar structure.

0.64 mm

Lo. Cretaceous Cupido Fm. Mexico Transverse section through a single, originally aragonitic, gastropod. All trace of original wall structure has been obliterated during inversion to calcite, but recognizable outline is preserved by internal and external sediment plus cement.

0.22

88

L o . Cretaceous Cupido Fm. Mexico

L o n g i t u d i n a l section of an o r i g i n a l l y aragonitic gastropod. A l l wall structure o b l i t e r a t e d but recognizable o u t l i n e is preserved, due largely to early diagenetic (probably synsedimentary) i n f i l l i n g of chambers w i t h fibrous cement crusts. Shell also i s o u t l i n e d by m i c r i t i z a t i o n of outer margin.

0.25 mm

J u r a s s i c Ronda u n i t of Subbetic Spain L o n g i t u d i n a l section of a high-spired gastropod. O r i g i n a l aragonite w a l l has inverted to c a l c i t e with loss of internal d e t a i l , yet original internal and external o u t l i n e s are f a i t h f u l l y preserved by m i c r i t i c sediment.

0.25 mm

P l i o c e n e Is.

Italy Section through part of the w a l l of a scaphopod, Dentalium sexangulare. T h i s group of m o l l u s k s i s characterized by i t s c o n i c a l shape, aragonitic s h e l l , and c o n c e n t r i c a l l y laminated crossed-lamellar w a l l structure. One can a l s o d i s t i n g u i s h numerous dark growth bands.

0.64 mm

mm

\'0>

89 Pliocene Is. Italy Close-up of w a l l structure of the scaphopod Dentalium sexangulare. External p l i c a t i o n s are v i s i b l e , and concentrically laminated crossedlamellar structure i s d i s p l a y e d along w i t h growth bands.

X.N.

0.22 mm

M i s s i s s i p p i a n Dartry L s . Ireland Cross section of a single cephalopod ( n a u t i l o i d ? ) . Size and shape are the primary distinguishing characteri s t i c s . In t h i s case, a l l chambers are f i l l e d w i t h sparry c a l c i t e cement.

1.24

M

Up. Cretaceous Fox Hi Us Ss. South Dakota •

T h i n - w a l l e d ammonite w i t h complete fibrous spar i n f i l l o f chambers. Ammonites are best recognized by their shapes—they are rarely a major rock-forming element. T h i s shell has homogeneous structure (prismatic and nacreous w a l l s are also known).

: M

fit' •«r*

*^M

X.N.

0.38

90 Pennsylvanian asphalt Oklahoma

Transverse section of a n a u t i l o i d cephalopod. N o t e the extensive c r u s h i n g of these uncemented and u n a l t e r e d ( s t i l l aragonitic) s h e l l s . Shows o r i g i n a l homogeneous prismatic and nacreous structures.

0.38 mm

Up. Cretaceous sediment New Jersey Cross section of central part of a belemnite rostrum showing r a d i a l l y arranged prismatic structure and massive construction.

X.N.

0.38 mm

Holocene sediment, 1000 meters

depth Coral Sea, P a c i f i c T r a n s v e r s e and o b l i q u e sections of modern pteropods (generally c l a s s e d w i t h the gastropods). Pteropods have a r a g o n i t i c s h e l l s w i t h conical shape and homogeneous prismatic wall structure.

X.N.

0.17 mm

91

Echinoderms

This page intentionally left blank.

93

Lo. and Mid. Pennsylvanian Marble Falls Ls. Texas Large crinoid ossicle showing typical characteristic of echinoderm grains—single-crystal extinction. Circular shape and central canal are common in many crinoidal grains. Note embayment by adjacent grains.

X.N.

0.38 mm

Up. Silurian part of TonolowayKeyser Ls. Pennsylvania Large and small crinoid fragments. Grains still retain single-crystal structure but microtexture is obliterated. Note central canal.

X.N.

0.38

iac> ~£ijgijt/&

fiSKL

Up. Mississippian Salem Ls. Indiana Longitudinal section of a crinoid stem showing a series of connected stem segments (columnals). It is quite unusual to find crinoid columnals still articulated. Also note axial canal in center, and unit extinction.

X.N.

0.37

94

Paleozoic crinoidal Is. United States

Crinoid arm plate shown as the nucleus of an ooid. The U-shape is characteristic of arm plates, and the single-crystal extinction and coarse porous structure identify the grain as being echinodermal.

0.06 mm

Up. Silurian part of TonolowayKeyser Ls. Pennsylvania Echinoderm fragment with singlecrystal structure an6 large overgrowth in optical continuity (syntaxial rim cement). Twin lines of calcite crystal are continuous from grain to cement.

X.N.

0.24 mm

Up. Silurian part of TonolowayKeyser Ls. Pennsylvania Crinoid fragment with single-crystal structure, and much of the internal part replaced by chert. Crinoid fragments are very susceptible to this type of replacement.

X.N.

0.38

95

,MC:M

Up. Eocene Ocala Fm. Florida

•

•

i

Large echinoderm fragment showing characteristic single-crystal extinct i o n and uniform granular microtexture (small pores f i l l e d w i t h " d i r t " ) . A l s o note early c a l c i t e overgrowth in o p t i c a l c o n t i n u i t y w i t h grain and later s i l i c a cement.

X.N.

0.30

Holocene sediment B e l i z e ( B r i t i s h Honduras) SEM v i e w of a fractured piece of e c h i n o i d w a l l . I l l u s t r a t e s the very solid, single-crystal construction and the network of large openings w h i c h transect the structure.

"Ill

SEM Mag. 1600X 7.8

HH

m„ :

>>"• »

•Hi

"

s

-&*; ^

,

:

"

'

•

•

•

•

•

.

,

,

Up. Cretaceous Upper Chalk England A large e c h i n o i d fragment in assoc i a t i o n w i t h Inoceramus prisms and planktonic Foraminifera. The range of p o s s i b l e fragment shapes from the d i s i n t e g r a t i o n of an e c h i n o i d is enormous, but all are i d e n t i f i a b l e through t h e i r e x t i n c t i o n behavior.

s:%l: ••'•

•

"'V*V • -;M;S^

S*:k? f

-

fxm

X.N.

0.30

96 L o . and Mid- P e n n s y l v a n i a n B l o y d Fm. Oklahoma L o n g i t u d i n a l section of an echinoderm spine. Note the bulbous a t t a c h ment area a t one end and the e l o n gate, r i b b e d , terminated spine i t s e l f . A s w i t h other e c h i n o i d grains, the e n t i r e spine is composed of a s i n g l e calcite crystal with unit extinction.

X.N.

0.20 mm

Holocene coral rubble beach sand B e l i z e ( B r i t i s h Honduras) Cross section of an echinoderm spine showing s i n g l e - c r y s t a l structure and very c h a r a c t e r i s t i c lacy pattern.

X.N.

0.24 mm

Holocene sediment Florida T h i s is a clorox residue of a modern H o l o t h u r i a n (sea cucumber). Embedded w i t h i n the f l e s h y t i s s u e o f these organisms are these s m a l l , irregular, perforated plates. Upon death and organic decay of the holot h u r i a n , these p l a t e s may be released to the sediment. F o s s i l examples are k n o w n , but are rare.

IOL<MM:^^} "*%&

0. 016 mm :

.

X>.

97

Trilobites and Ostracods

This page intentionally left blank.

99 Up- Ordovician Reedsvil le Shale Pennsylvania Several trilobite fragments in a sandy matrix. Grains show f i n e , u n i form structure w i t h e x t i n c t i o n bands (in polarized light) which sweep across the grain as the stage i s rotated.

X.N.

0.38 mm

M i d . Silurian Rochester Shale New York Single t r i l o b i t e fragment w i t h t y p i c a l convoluted shape (and tumed-under end), uniform skeletal structure, and e x t i n c t i o n bands. Some alteration apparent.

X.N.

0.30 mm

Up- Ordovician R e e d s v i l l e Shale Pennsylvania L a r g e t r i l o b i t e fragment in center of photo shows f i n e perforations (canali c u l i ) f i l l e d w i t h m i c r i t i c sediment. Shell w a l l s t i l l shows uniform or homogeneous prismatic structure and sweeping e x t i n c t i o n .

0.25 mm

100 Eocene Green River Fm. Wyoming Ostracodes. Note thin w a l l s , small s i z e , and shell shape. The t h i n w a l l e d nature of the carapace i s often a c h a r a c t e r i s t i c indicator of freshwater forms.

0.38

Up. M i s s i s s i p p i a n H m d s v i l l e L s . Oklahoma Section of a single valve of an ostracode. T h i s group is characteri z e d by small size (average 0.50.75 mm in p o s t - P a l e o z o i c forms and 1-2 mm in P a l e o z o i c ones), homogeneous p r i s m a t i c w a l l structure w i t h a c a l c i t e and c h i t i n composit i o n , and a shape l i k e a pelecypod. D i s t i n g u i s h e d from pelecypods by smaller size and homogeneous w a l l structure.

0.07 mm

Up. M i s s i s s i p p i a n H i n d s v i l l e L s . Oklahoma Cross section of a s i n g l e ostracode v a l v e , i l l u s t r a t i n g the homogeneous prismatic w a l l structure w i t h sweeping e x t i n c t i o n , the small but t h i c k shell, and the t y p i c a l V-shaped carapace t e r m i n a t i o n .

X.N.

0.05 mm

101 M i s s i s s i p p i a n Is. Ireland

A pair of ostracode valves showing common overlap of one valve over the other, as w e l l as the recurved termination of one v a l v e .

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0.027 mm

i 1 ?*;£*•

Holocene sediment B e l i z e ( B r i t i s h Honduras) SEM v i e w of one surface of an o s t r a code, probably of the genus Cativella, showing irregular carapace o u t l i n e w i t h small perforations and spiny p r o t r u s i o n s .

M 4

1

SEM Mag. 100X 125 (im

103

Plant Fragments

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105 P e n n s y l v a n i a n Mazon Creek coal balls Illinois P a r t o f an H F a c i d acetate peel of a s i l i c i f i e d bed of plant f o s s i l s . T h i s i s the seed (Pachytesta) of the P a l e o z o i c pteridosperm M e d u l l o s a . Note the preservation of the c e l l u l a r structure—distinguished from red algae by much coarser c e l l s i z e .

0.25 mm

*T£CT*

P e n n s y l v a n i a n Mazon Creek coal

balls .Illinois P a r t of an H F a c i d acetate peel. Shows moderate preservation of c e l l u l a r structure in Stigmaria, a root of L e p i d o d e n d r a l e s . Note radia t i n g rays of c e l l u l a r t i s s u e and curved, irregular l i n e s which mark s i l i c a replacement f r o n t s .

0.64;

O i i g o c e n e Creeds Fm. Colorado B r o w n i s h w i s p s i n center of photo are small pieces of p l a n t material l y i n g p a r a l l e l to bedding. The color of such organic matter depends upon the degree of thermal a l t e r a t i o n the rock has seen ( y e l l o w at very low temperatures to black at very high temperatures).

0.04 mm

106 Up. Cretaceous Red Bank Sand New Jersey

Stained palynological preparation showing a single trilete spore. A l though these grains can be seen in thin sections of carbonate rocks, they are much more easily seen in stained insoluble residues. They can be used in stratigraphic as well as environmental studies.

0.018 mm

Up„ Cretaceous Red Bank Sand New Jersey Stained palynological preparation showing a single spore of Sphagnum (a moss). These grains are noncalcified and consist entirely of organic matter.

0.018 mm

Up. Cretaceous Mount Laurel Sand New Jersey Stained palynological preparation showing a single pollen grain of Pinus. T h i s is a typical bissacate form.

0.018 mm

107 L o . Cretaceous Dakota Group Colorado

SEM view of a s i n g l e t r i l e t e fern spore, Appendicisporites sp. A l though these grains are hard to see in normal SEM photos of carbonates, they are frequently apparent in i n s o l u b l e residues.

SEM Mag. ca. 2000X

6.2 jam

L o . Cretaceous Dakota Group Colorado SEM v i e w of a simple t r i l e t e spore, Cyatbidites sp. which i s p a r t i a l l y c o l l a p s e d . T h e 3 r a d i a t i n g tetrad scars are c l e a r l y v i s i b l e .

SEM Mag. 2000X

6.3

fin

L o . Cretaceous Dakota{?) Group Colorado SEM view of two t r i c o l p a t e angiosperm pollen grains, Tricolpites sp. w i t h the pollen apertures v i s i b l e .

SEM Mag. ca. 1000X

12.5 Mm

108 iimigfin

L o . Cretaceous Dakota Ss. Colorado SEM view of a single angiosperm pollen grain, pites sp. It shows a pair pollen apertures as w e l l t i c u l a t e d surface of small

SEM Mag. ca. 2000X

tricolpate Retitricolof bowed as a repores.

6.0 fxm

/

1

109

Other Carbonate Grains Pellets

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111 L o . and M i d . Ordovician D e e p k i l l Shale New York A p e i s p a r i t e . Abundant p e l l e t s of unknown, but probably f e c a l , o r i g i n ; cemented by sparry c a l c i t e . Note the u n i f o r m i t y of grain s i z e and shape.

0.38 mm

Holocene sediment Mexico Two p e l l e t s from a modern lagoonal s e t t i n g . These are fecal p e l l e t s in all p r o b a b i l i t y and show the common rounded, rod-shaped o u t l i n e of fecal p e l l e t s . In t h i s sediment, the u n i formity of s i z e and shape of p e l l e t s aids in their i d e n t i f i c a t i o n as being of fecal o r i g i n .

0.09 mm

J u r a s s i c Ronda unit of Subbetic Spain A Favreina sp. p e l l e t . Note the regular arrangement of h o l l o w tubules w h i c h are formed by elongate appendages from the i n t e s t i n a l w a l l s . In the H o l o c e n e , such p e l l e t s are produced by anomuran crustaceans. These p e l l e t s can be found as major rock-forming elements in J u r a s s i c and Cretaceous limestones.

0.17 mm

112 Up. J u r a s s i c Smackover Fm. Alabama Another Favreina sp. p e l l e t showing a different pattern of internal tubules These p e l l e t s have been subdivided into numerous species and have been used for stratigraphic zonation.

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113

Ooids and Pisolites

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115 Pleistocene(?) dunes Bahamas

Modern marine ooids are generally aragonitic, range in size from about 0.1 to 1 mm, and have a tangential arrangement of c r y s t a l s which y i e l d the type of pseudo-uniaxiai cross seen here. Nuclei are varied and can include carbonate or noncarbonate grains. Deposits are often w e l l sorted and form in h i g h l y a g i t a t e d , bank margin environments in open marine, marginal marine, or lacustrine s e t t i n g s .

X.N.

0.11 mm

Holocene sediment Great Salt L a k e , Utah These o o i d s show the textures commonly found in h y p e r s a l i n e lakes. Most grains have coarse, r a d i a t i n g c r y s t a l s of bladed to fibrous aragon i t e interspersed w i t h layers of tangential, very f i n e l y c r y s t a l l i n e aragonite. T h e radial texture appears to be d i s r u p t i v e and therefore secondary. Such h y p e r s a l i n e lake deposits commonly have a very high percentage of broken grains.

0.10 mm

Holocene sediment Florida These ooids were formed syntheti c a l l y in a water p u r i f i c a t i o n plant (thus without algal influence). N u c l e i are quartz and g l a u c o n i t e w h i l e the o o l i t i c layers are coarse, r a d i a l l y oriented blades of probable c a l c i t e . Note the s i m i l a r i t y in texture to the Great Salt L a k e o o i d s .

X.N.

0.25 mm

116

Lo. and Mid. Pennsylvanian Bloyd

Fm. Oklahoma Superficial oolitic coatings on echinoderm fragments, These are thin (one to five layer) concentric coatings which must be carefully distinguished from micrite envelopes. They are important in echinodermal limestones as they isolate the grains from pores, preventing cementation by overgrowths. Common in moderately agitated waters. Note thickened coatings in embayed areas; this is typical of oolitic growth.

0.25 mm

Holocene sediment Laguna Madre, Texas The relatively high salinity and moderately low energy environment of Laguna Madre and Baffin Bay, Texas produces superficial ooids with alternating layers of aphanocrystalline aragonite and lighter, coarser, radial high-Mg calcite (both seen here). The coatings are generally thin and often incomplete.

X.N.

0.07 mm

Holocene sediment Laguna Madre, Texas This illustrates an incomplete, eccentric oolitic coating which occurs commonly on grains from low energy oolite forming areas. The aragonitic coatings are quite thick, but only cover a portion of the grain. The rest of the grain was probably resting in the bottom sediment and agitation was insufficient to rotate the grain.

X.N.

0.09 mm

117 Holocene sediment Bahamas

SEM v i e w of the surface of a modern aragonitic o o i d from an open-marine s e t t i n g . The small aragonite needles w h i c h make up the ooid are seen to be oriented w i t h their long axes tangential to the outer surface of the o o i d , but randomly oriented w i t h i n that curved plane. The large holes are probably algal borings.

SEM Mag. 10,000X

1.3 Mm

Holocene sediment J o u l t e r s Cay, Bahamas T h i s is a common stage of a l t e r a t i o n of modern o o i d s . Small portions of the o r i g i n a l structure can be seen, but most of the grain has been o b l i t erated by the formation of empty tubes by the boring of algae and other organisms. A s these tubes are f i l l e d w i t h f i n e - g r a i n e d sediment or cement, the o o i d takes on a m i c r i t i z e d appearance (lower part).

0.05 mm

Up. Cambrian K i t t a t i n n y L s . New Jersey The textural d e t a i l s of ooids can also be lost during later d i a g e n e s i s , as in t h i s case, where a l l internal structure has been o b l i t e r a t e d by d o l o m i t i z a t i o n . Grains are i d e n t i f i e d as ooids on the basis of s i z e , shape, and s o r t i n g . Note lack of s e l e c t i v i t y in replacement.

0.38 mm

118 Up. Mississippian Pitkin Ls. Oklahoma A very common texture in ancient ooids is the development of a radial fabric of the type seen here. A l though the concentric laminations are still clearly visible, they are cut by occasional thin, disruptive radial crystal s. This may be produced during alteration from original aragonite to later calcite,, Also note spat ling of outer cortex of one ooid.

0.09 mm

Up. Cambrian and Lo. Ordovician Gallatin Fm. Wyoming These ooids show no internal structure and are classed as ooids only on the basis of shape, size, and sorting. They most probably underwent dissolution in which the ooids were removed (producing oomoldic porosity) and the resulting voids were later filled with coarse (often single-crystal) sparry calcite.

0.38 mm

Lo. and Mid Pennsyl vanian Bloyd

Fm. Oklahoma These ooids have suffered a complex sequence of alteration. They were completely dissolved during the alteration from aragonite to calcite and also have been strongly sheared, yielding a " s p a s t o l i t h " texture. The outer cortex layers have been sheared off to produce what looks like a series of linked grains.

0.04 mm

119

Lo. Ordovician West Spring Creek Fm. Oklahoma This pisolite (larger than 2 mm) has a nucleus and vague concentric laminations consisting of Girvanella algal tubules. The grain would thus be classed as an oncolite. Definite evidence of algal origin of pisolites is often considerably more difficult to see.

0.11

Holocene sediment Carlsbad Caverns, New Mexico An example of a "cave p e a r l " , an inorganically formed pisolite found on cave floors. It shows coarse, fibrous calcite crystals growing in radially oriented fan-shaped clusters interspersed with thin rinds of gypsum.

X.N.

0.25 mm

Quaternary sediment

Abu Dhabi A portion of a coastal caliche deposit, this rock has large pisolites with well developed coatings set in a laminated crust. Yet, because of the marine and hypersaline-evaporitic pore waters in the Persian Gulf area, these vadose deposits are composed of aragonite and high-Mg calcite. Unlike other caliche, therefore, they are subject to extensive later alteration.

X.N.

0.25 mm

120 Quaternary caliche Texas A calcific, irregularly laminated caliche pisolite with abundant quartz inclusions^ Caliche pisolites are characterized by irregular lamination, inclusions, complex nuclei, autofracturing, microstalactitic textures, interlocking grains, and inverse grading of pisolite sizes within a single bed.

0.64

Lo. Pennsyl vanian Hale Fm. Oklahoma This photo is included to show that some cementation and recrystallization features can produce textures at least superficially similar to oolitic and pisolitic ones* Here, early cement rims surround grains and contrast with later ankeritic cement.

0.25 mm

Permian Phosphoria Fm. Idaho All ooids and pisolites are not composed of carbonate. Phosphate, hematite, goethite, chamosite, barite and other ooids are known. Those shown here are phosphatic. In many cases, however, phosphatic and iron pisolites or ooids form by replacement of earlier carbonate ones.

0.38 mm

121

Intraclasts and Extraclasts

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123 M i d . Ordovician (frm?) Virginia

I n t r a c l a s t s . L a r g e , rounded grains w i t h internal structure (and encomp a s s i n g f i n e grains) are c l e a r l y reworked carbonate sediments but probably were deposited in the same d e p o s i t i o n a l c y c l e as the f i n a l s e d i ment—thus they are i n t r a c l a s t s .

0,24 mm

Holocene sediment Berry I s l a n d s , Bahamas A modern i n t r a c l a s t of the " g r a p e s t o n e " t y p e . These are c l u s t e r s or aggregates of other grains ( s k e l e t a l fragments, o o i d s , p e l l e t s , etc.) held together by cement and a l g a l , foraminiferal, and other encrustation. Grapestone forms in areas of mod= erate or i n t e r m i t t e n t a g i t a t i o n where cementation can take p l a c e but where reworking prevents formation of complete c r u s t s .

0.22 mm

L o . Cretaceous Cupido Fm. Mexico An a n c i e n t example of a grapestone d e p o s i t . Note the c l u s t e r s of cemented ooids w i t h a botryoidal external shape as w e l l as the isopachous crust of submarine cement w h i c h surrounds a l l g r a i n s .

0.25 mm

Lo. Cretaceous Glen Rose |_s. Texas Although these grains look very much like intraclasts, they are actually the fillings (steinkerns) of Corbula sp», a pelecypod. Note the consistent teardrop shape. The complexity of internal filling textures is probably the result of rolling of the grains during infilling.

0.64 mm

Eocene Oberaudorf Schichten Austria An example of a calclithite, a rock composed of extraclasts. These grains are detrital from older limestones within the rising Alpine region. Note the polymict character of the grains—they include spicular cherts, dolomites, and several types of limestone. Because of the solubility and low abrasion resistence of carbonate grains, such deposits are generally associated with major fault scarps or very arid climates.

X.N.

0.64 mm

125

Peloids

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127 Pleistocene(?) dunss Bahamas T h i s photograph and the f o l l o w i n g three show the progressive a l t e r a t i o n of grains ( w i t h l o s s of c h a r a c t e r i s t i c textures) w i t h i n the depositional sedimentary environment. These are r e l a t i v e l y fresh and unaltered ooids i l l u s t r a t i n g strong birefringence and a pseudo-uniaxial cross.

X.N.

O.l 1 mm

Holocene sediment Joulters Cay, Bahamas T h i s is the same type of ooid as in the previous photo, but it has undergone considerable algal and fungal boring. Most of the borings are s t i l l u n f i l l e d , showing their tubular shape, but some have been f i l l e d and thus appear as d i f f u s e m i c r i t i c patches.

0.05 mm

Holocene sediment J o u l t e r s Cay, Bahamas These ooids have undergone even more boring. Although a few tubules are s t i l l v i s i b l e , most of the grain now has a uniform m i c r i t i c texture w i t h some areas of largely unaltered structure at the centers.

0.11 mm

128

Holocene sediment Joulters Cay, Bahamas

An example of a probable ooid which has been virtually completely micritized. Although the section may be somewhat tangential to the ooid, no remnant structure is visible in this cut and the grain would have to be classed as a peloid. Other than size and shape, no textural characteris tics would allow identification as an ooid.

0.09 mm «

Up. Oligocene Suwannee L s. Florida This sediment has a high percentage of micritized grains. Although a few are still recognizable as miliolid Foraminifera, grapestone, or shell fragments, many have lost all recognizable features and would have to be grouped as peloids.

G.P.

0.38 mm

Up. Jurassic Solnhofen Ls. Germany A pelletal sediment which shows considerable irregularity of " p e l l e t " size. Are some of these grains peloids produced by the micritization of other grains; are they intraclasts; or are they pellets of a number of different organisms?

0.25

' ' •

'.

S»«

129

Other Minerals Dolomites and Evaporites

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131

Mid. Eocene Coamo Springs Ls. Puerto Rico Large ankeritic (iron-rich) dolomite rhombs clearly associated with a fracture in a red algal grain. The association with both fractures and red algae is a common one for dolomite.

X.N.

0.38 mm

Mid. Eocene Avon Park Ls.. Florida Finely crystalline dolomite replacement of the micritic matrix of a former biomicrite. Fossil fragments were not doiomitized and have been subsequently dissolved, leaving moldic porosity.

X.N.

0.38 mm

Lo. Ordovician Stonehenge Ls. Pennsylvania Coarse replacement dolomite (note euhedral rhombic outline of crystals), Intercrystalline porosity in such rocks can be very high.

X.N.

0.38 mm

132

Up Permian Tartsill Fm. New Mexico The dark areas in this section are micritic and pisolitic sediments which have been replaced by aphano* crystalline dolomite considered to have been virtually penecontemporaneous. Light-pink stained areas are later sparry calcite. Such dolomite is very difficult to recognize without staining or chemical analysi s,

0,64 mm

Lo„ Ordovician Ellenburger Ls. Texas A medium crystalline replacement dolomite showing considerable iron zoning. Note the consistency of zonation from crystal to crystal, in* dicating that crystals formed simultaneously and during a period of uniformly fluctuating conditions.

0.11 mm

Up- Cretaceous Chalk France A tightly interlocked, mediumcrystalline, complete replacement dolomite with considerable zonation. This dolomite probably formed rather late in the history of the sediment and is recognizable as dolomite on the basis of both the euhedral crystal shapes and the internal zonation.

0.11 mm

133 U p . Permian C a s t i l e Fm. New Mexico

A bedded and varved gypsum deposit. A t the top of the photo is a lamina of carbonate w h i l e the rest of the s l i d e shows interlocking crystals and crystal fragments of gypsum. In the deeper subsurface t h i s rock is anhydrite and probably has inverted to gypsum in near-surface areas. Note characteristic low birefringence

X.N.

0.38 mm

M i s s i s s i p p i a n upper Debolt Fm. Canada

Gypsum c r y s t a l s as replacement of or displacement of m i c r i t i c sediment. Note the low birefringence and chara c t e r i s t i c crystal shapes of these gypsum grains. Several have been replaced by c a l c i t e spar w h i l e s t i l l ret a i n i n g their crystal o u t l i n e .

X.N.

0.25 mm

M i d . Pennsylvanian Paradox Fm.

Utah Several large replacement c r y s t a l s of gypsum. L o w birefringence and crystal shape are d i a g n o s t i c , w h i l e presence of abundant carbonate i n clusions is common in the case of replacement grains. Gypsum must be c a r e f u l l y d i s t i n g u i s h e d from a u t h i genic quartz, and can be lost through prolonged or improper t h i n - s e c t i o n grinding.

X.N.

0.25 mm

134

Lo. Cretaceous Ferry |_ake(?) Anhydrite Texas Fine-grained "chicken-wire" anhydrite replacement of micritic sediment. Shows "auto fractured" crystal fragments in a nodular texture with interspersed, displaced original micritic sediment. Anhydrite can be lost from thin sections unless they are carefully (and rapidly) prepared.

X.N.

0,38 mm

Lo. Cretaceous Ferry Lake Anhydrite Texas Fibrous to bladed filling the central pulid worm tube. anhydrite replaces walls.

X.N.

anhydrite shown cavity of a serCoarse euhedral the serpulid tube

0.38 mm

Lo. Cretaceous Glen Rose Ls. Texas Because of the high solubility of most evaporites they are very susceptible to postdepositional removal by leaching. Yet even in those cases, evidence can be seen for the original presence of evaporites. In this example it takes the form of clear molds with euhedral crystal outlines, probably of anhydrite. Pink areas are now voids.

G.P.

0.25

135 Lo. Cretaceous Glen Rose L s . Texas

Celestite (SrSO^j) filling large vugs in a sparse biomicrite. Celestite formation is often associated with early supratidal diagenesis (releasing Sr from aragonite), Celestite shows very low (first-order) colors.

X.N.

0.38 mm

Mid. Devonian Keg River equivalent Canada

Halite is rarely found in outcrop samples but can be present in subsurface materials. It is isotropic and thus difficult to recognize. However, the presence of intersecting cleavages at right angles and inclusions within what otherwise looks like pore space is indicative of halite. Halite is commonly lost during thin section preparation unless sections are ground in o i l .

0.37 mm

137

Silica Minerals

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139 Up. Cambrian Copper Ridge DoU and Conococheague L s . Virginia Well-rounded d e t r i t a l quartz sand grains scattered throughout a dolom i t i z e d carbonate mudstone. Quartz grains are at various stages of extinction, but none show colors higher than f i r s t order.

X.N.

0.38 mm

Eocene deep-water ooze Bermuda R i s e , North A t l a n t i c Ocean

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Opaline diatom (large c i r c u l a r grain w i t h i n t r i c a t e pattern) and opaline sponge s p i c u l e fragment (lower right center). A large percentage of the chert in sedimentary rocks is derived from the d i s s o l u t i o n and reprec i p i t a t i o n of biogenic opal from diatoms, r a d i o l a r i a n s , sponges, and other organisms.

m

0.016 mm

v— I f -*

Up- Silurian part of Tonoloway-* Keyser L s „ Pennsylvania A chert ( m i c r o c r y s t a l l i n e quartz w i t h included water bubbles) replacement of the central portion o f a c r i n o i d fragment. Chert is a very common replacement and cementation mineral in carbonate r o c k s .

X.N.

0.30 mm

140 M i d . Eocene Coamo Springs L s . Puerto Rico

S i l i c a replacement of part of a m o l lusk fragment. T h i s is a coarse fibrous chalcedony/megaquartz texture w h i c h clearly crosscuts primary skeletal fabric.

X.N.

0.38

Up. Cambrian Copper Ridge D o l . and Conococheague Virginia A u t h i g e n i c quartz crystal in a c a t c i t e v e i n . P o s i t i o n in vein i n d i c a t e s certain authigenic o r i g i n , and the perf e c t l y euhedral termination i s chara c t e r i s t i c of such authigenic minerals.

X.N.

0,08 mm

M i d . Pennsyl vanian Paradox Fn Utah Coarse replacement of a bivalve w a l l by authigenic quartz. C r y s t a l s retain many carbonate i n c l u s i o n s and extend from shell w a l l into the surrounding m a t r i x . S i l i c a replacement is often very s e l e c t i v e and is commonly a s s o c i a t e d w i t h microenvironments in and between shells or in other areas of higher organic content.

X.N.

0.25 mm

WMLB&B&SBfcX

141 Up. J u r a s s i c Zuloaga Fm. Mexico

E x t e n s i v e a u t h i g e n i c quartz replacement. Note that most of the a u t h i genic quartz c r y s t a l s d i s p l a y e x c e l lent c r y s t a l terminations but have enormous central cores of almost completely undigested carbonate.

0.25 mm

Up. Cambrian Mines Dolomite Mbr. of Gatesburg Fm. Pennsylvania Complete s i l i c a replacement of an o r i g i n a l l y carbonate ( o o l i t i c ) s e d i m e n t Note quartz overgrowths on nuclei of o o i d s , chert replacement of ooids and part of matrix, chalcedonic i n f i l l i n g of former v o i d s , and coarse megaquartz vein at bottom of photo. A complete range of s i l i c a fabrics thus can be found even in small areas.

X.N.

0.38:

U p . Cambrian Copper Ridge D o l . and Conococheague L s .

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Virginia Multiple diagenetic generations. Chert ( b l a c k - s p e c k l e d background in t h i s photo) replaced original limestone. Later, euhedral dolomite rhombs grew in chert. F i n a l l y , dolomite and chert are cut by megaquartz v e i n s .

X.N.

0.08 mm

142 Eocene Green River Fm. Wyoming

Carbonate ooids cemented (and partly disrupted) by coarse c h a l cedonic q u a r t z . Chalcedonic quartz is normally a v o i d f i l l i n g fabric.

X.N.

0.38

Up. Eocene Ocala L s . Florida Chert cementation (partial) of a carbonate grainstone. Chert is j u s t beginning to fringe carbonate grains (including large Foraminifera in center).

X.N.

0.30 mm

L o . Permian Getaway L s . Mbr. of Cherry Canyon Fm. Texas Chalcedonic quartz i n f i l l i n g of a calcareous sponge. Note the w e l l developed r a d i a t i n g bundles of chalcedony f i b e r s cut by uniform growth banding, as w e l l as the growth i n terference between a d j a c e n t chalcedony bundles.

X.N.

0.64 mm

143 U p . Cretaceous C r a i e grise Netherlands

SEM v i e w of s i l i c e o u s area w i t h i n c h a l k . The photo shows small spherules (sometimes c a l l e d lepispheres) of c r i s t o b a i i t e . Recent work has shown that the a l t e r a t i o n of opal to quartz chert generally goes through the intermediate stage of C r i s t o b a l i t e , and that the t r a n s i t i o n s between these three phases are largely temperature c o n t r o l l e d .

SEM Mag,5000X

2.6

fim

Up. Cretaceous Monte A n t o l a Fm. Italy A u t h i g e n i c feldspar r e p l a c i n g limestone. A l b i t e is most common replacement although other types are known. Recognized on basis o f c r o s s c u t t i n g texture and euhedral or twinned o u t l i n e (not w e l l shown here) as w e l l as by the presence of carbonate i n c l u s i o n s . Rarely forms a large percentage of the sediment.

X.N.

0.04 mm

145

Iron Minerals

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147 M i d . Silurian C l i n t o n F m . Pennsylvania

Hematite o o l i t i c coatings on carbonate grains ( f o s s i l fragments). These coatings are good indicators of s h a l l o w , a g i t a t e d water (and in this c a s e , form an economic iron d e p o s i t ) . Hematite may be after chamosite, w h i c h was a replacement of o r i g i n a l carbonate.

X.N.

0.24 mm

L o . Cretaceous Glen Rose L s . Texas Hematite f i l l i n g pore space between internal f i l l i n g s of small Corbula (pelecypods). Hematite is d i s t i n guishable from other opaque minerals ( p y r i t e , m a g n e t i t e , e t c ) under ref l e c t e d l i g h t . Under very strong transmitted l i g h t hematite may show t y p i c a l blood-red color.

0.30

M i d . Silurian C l i n t o n Fm. Pennsylvania Dense hematite cement w i t h abundant quartz s i l t grains and t r i l o b i t e fragments. T h i s was an economic iron ore.

X.N.

0.38 mm

148 Jurassic Etsenoolith Germany Hematite ooids illuminated with conoscopic condenser in place—gives very intense transmitted l i g h t which shows r e d d i s h - y e l l o w color of t h i s s l i g h t l y weathered hematite. These were originally carbonate ooids w h i c h were replaced by various iron minerals.

0.24 mm

Up. Cretaceous Monte A n t o l a Fm. Italy

. . : ' • * ' . • ; . " .

A p y r i t e grain in transmitted l i g h t . Although some detritai p y r i t e can be found in carbonates, most is a u t o g e n i c . It is often found as spherules (framboids) a s s o c i a t e d w i t h patches of o r g a n i c matter or f o s s i l s , because i t forms under reducing conditions where sulfur i s present.

CLIO mm

«£&£•*.*.»

Up.. Cretaceous Monte A n t o l a F m . Italy Photographed w i t h a combination of reflected and transmitted l i g h t , t h i s example shows a burrow f i l l e d w i t h framboidal p y r i t e and surrounded by an a l t e r a t i o n halo of l i m o n i t e . P y r i t e in a s s o c i a t i o n w i t h burrows is common because of the high organic content of such structures.

R.L.

0.04 mm

149

Up. Cretaceous Chaik B r i t i s h North Sea

SEM view of a p y r i t e framboid. Note the c l u s t e r of small interlocking c r y s t a l s and the smooth, almost perfectly spherical exterior. These can form singly or in groups as an authigenic product.

«f' •

•••?:

«**.«%

•*>»

A

S E M M a g , 4300X

3/xr

151

Phosphate and Glauconite

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153 Up. Cretoceous San C a r l o s Fm. Texas

A phosphatic shell fragment (made of cellophane) in a s i l t y carbonate sediment Phosphate typically shows a brownish color in transmitted plane l i g h t

0.24 mm

Up. Cretaceous San Carlos Fm. Texas Same as above photo but with polarized l i g h t to show the very low order (virtually isotropic) interference colors t y p i c a l of phosphate ( c e l l o phane grains.

X.N.

0-24 mm

*"**1^L,: *T

L o . T e r t i a r y sediment Texas Section of a p i e c e of phosphatic bone material (collophane) w i t h a very common cross-fibrous texture, and the very low order interference colors.

X.N.

0.38 mm

154

Up. Cretaceous Navesink Fm. New Jersey

Large, rounded glauconite grains in a glauconitic marl. These may have a fecal pellet origin. Green color and speckled greenish birefringence are characteristic for this mineral.

X.N.

0.38 mm

Up. Cambrian Meagher Fm. Montana Angular glauconite grains showing typical very fine granular texture and dark green color. The angularity indicates these glauconite grains may have been formed by alteration of detrital biotite.

X.N.

0.06 mm

155

Carbonate Cements

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157 Holocene beachrock Bahamas

Uniform fringe of fibrous aragonite cement around o o l i t i c and m i c r i t i z e d grains. The needle character and uniform (isopachous) f r i n g i n g are c h a r a c t e r i s t i c of lower intertidal and submarine cement.

X.N.

0.24 mm

Holocene beachrock Bahamas Closeup of uniform isopachous fringe of fibrous arayoni fe-needle cement holding together oolitic g r a i n s . Fringe smoothly f o l l o w s outl i n e of voids and is not concentrated near grain j u n c t i o n s as in some vadose cements.

0.06 mm

Quaternary sediment

Abu Dhabi F r i n g i n g cements of aragonite ( l i g h t c o l o r e d , radial fibrous crystals) and later high-Mg calcite (micritic) cement. The mineralogies, compos i t i o n s , and c r y s t a l morphologies are those of cements produced from seawater while the depositional textures (meniscus and m i c r o s t a l a c t i t i c ) are vadose. T h i s r e s u l t s from the f a c t that vadose waters in Abu Dhabi sabkhas are marine to hypers a l i n e in c o m p o s i t i o n .

X.N.

0.22 mm

158 Quaternary sediment Abu Dhabi

Complete cementation of pore space by aragonite needles w i t h small amounts of high-Mg c a l c i t e . Modern submarine and i n t e r t i d a l sediments can be f u l l y cemented in the d e p o s i t i o n a l environment. However, both the primary grains and the cements are of unstable mineralogies and the rock is l i k e l y to undergo very s i g n i f i c a n t future diagenetic m o d i f i c a t i o n w i t h p o s s i b l e improvement of porosity. X.N.

0.25

Holocene sediment B e l i z e ( B r i t i s h Honduras) Submarine aragonite-needle cement forming isopachous l i n i n g s of voids w i t h i n a coral s k e l e t o n . Note irregular but b a s i c a l l y radial arrangement of f i b e r s .

SEM

Mag. 3000X

4.1

pm

Holocene sediment, Tobacco Cay B e l i z e ( B r i t i s h Honduras) Cemented internal sediment w i t h i n voids in a coral s k e l e t o n . Cement is p e l l o i d a l high-Mg c a l c i t e lime s i l t (stained red w i t h C l a y t o n Y e l l o w ) . Sediment is less than 500 years o l d and i s from the barrier reef crest. Photo courtesy of R. N. Ginsburg.

0.17

;

^*>?

mm

m

*

*-

/

159

— a — . .

••;•

:.

. • •

••

,

Jp.,;|j|p.,. "' ' ' MifBjt''

...

Holocene sediment. Tobacco Cay B e l i z e ( B r i t i s h Honduras) "

•I •

D e t a i l of a large area of cemented internal sediment of pelloialal h i g h Mg c a l c i t e lime s i l t stained red w i t h Clayton Y e l l o w , Such cementation is v o l u m e t r i c a l l y very important in the cementation of many modern reefs and other s h a l l o w marine sediments. Photo courtesy of R. N . Ginsburg.

0.09 mm

Holocene sediment V i r g i n Islands (St. Johns)

«i

SEM v i e w of a high-Mg c a l c i t e rim cement. In thin section these s m a l l , equant c r y s t a l s appear very s i m i l a r to a m i c r i t i c or p e l l e t a l c o a t i n g . Only through scanning electron microscopy can one resolve the excellent crystal terminations. This cement is from a shallow marine setting.

S E M M A G . 3000X

4.1 Mm

M r

Quaternary sediment, Tobacco Cay B e l i z e ( B r i t i s h Honduras) Cementation of large voids in barrier reef w a l l . F i b r o u s aragonite is arranged in dense, botryoidal arrays interlayered w i t h gray marine sediments and red-stained high-Mg c a l c i t e cement and sediment. Sediment is about 12,000 years o l d . Photo courtesy of R. N . G i n s b u r g .

; r ;t

***""'. *K.-&

>.

M

- ••

Scale shown on photo

160 Quaternary sediment, Tobacco Cay B e l i z e ( B r i t i s h Honduras) Cementation of large voids in reef w a l l of barrier reef. Shows dense botryoidal a r a g o n i t e in a s s o c i a t i o n w i t h red ( C l a y t o n Y e l l o w stained) high-Mg c a l c i t e cement. Note dark, e l l i p t i c a l borings of marine organisms w h i c h cut cement.. T h i s is exc e l l e n t e v i d e n c e for s y n d e p o s i t i o n a l cementation. Sediment is less than 12,000 years o l d . Photo courtesy of R. N . G i n s b u r g .

X.N.

Scale shown on photo

'-*> rze&ar, Up. Cretaceous White Northern Ireland

Ls..

T h i s is a hardground or s y n s e d i mentary l i t h i f i c a t i o n s u r f a c e . These form during breaks in sedimentation and r e f l e c t , in some areas, lowered sea level (but not subaerial exposure). The sediment on the right has been cemented w i t h carbonate, phosphate, and glauconite and is bored, e n c r u s t e d , and eroded into pebbles (upper l e f t ) . I t i s important to dis» t i n g u i s h such submarine hiatuses from unconformities produced by subaerial exposure and e r o s i o n . Enc r u s t a t i o n and repeated boring by marine organisms coupled with marine cements are the important c r i t e r i a for p r o v i n g submarine o r i g i n . 0.64 mm

Holocene dune sands Mexico Meniscus cement. Note that cement i s found only at grain contacts (presumably where meniscus water f i l m s were trapped)~no complete c a v i t y i i n i n g s . T h i s type of cement i s chara c t e r i s t i c o f vadose c e m e n t a t i o n . C r y s t a l s are c a l c i t e precipitated from freshwater.

X.N.

0.10 mm

161 Quaternary sediment J o u l t e r s Cay, Bahamas An example of e x t e n s i v e freshwater cementation, probably w i t h i n the vadose environment. Note the formation of a blocky c a l c i t e mosaic with r e l i c t meniscus texture and the lack of d i s s o l u t i o n features on the s t i l l - a r a g o n i t i c grains. L a t e r d i a genesis of the rock may y i e l d molcic porosity.

'. m V • v

•&£•

i

0.11 •

Quaternary crust Abu Dhabi A modern example of m i c r o s t a l a c t i t i c cement on a m o l l u s k . The cement (here aragonite and high-Mg c a l c i t e , but more commonly low-Mg c a l c i t e ) hangs as pendulous bulges from the undersides of grains. T h i s is c l e a r l y the product of the concentration of water drops on the bottoms of g r a i n s . Such cement, o c c a s i o n a l l y termed pendulous or g r a v i t a t i o n a l cement, is c h a r a c t e r i s t i c of vadose exposure.

w

u • • ' : • • •

-;••

•*t-'JtA/4

™ X.N.

0.25

Up. Permian T a n s i l l Fm. New Mexico An ancient example of preserved m i c r o s t a l a c t i t i c cement. Note the s l i g h t corrosion of the upper surfaces of grains and the thick cement crusts on the undersides of grains or internal voids in the Mizzia g r a i n stone. The green areas are voids f i l l e d w i t h stained p l a s t i c .

0.64 mm

162

Cretaceous El Abra Fm. Mexico Small leached voids of this dismicrite fabric are filled with a geopetal crystal silt{vadose silt) which commonly is found in sediments which have been exposed to vadose diagenesis. The filling of leached voids and the crystal size and shape of the silt are the diagnostic features in this key to subaerial exposure.

0.64 mm

Pleistocene Key Largo Ls. Florida A partially leached void filled with low-Mg calcite whisker crystal cement. These are thin, randomly oriented calcite crystals which have been found in a number of modern localities. They are produced in meteoric waters, probably within the vadose zone, but are not commonly recognized in ancient environments.

X.N.

0.38 mm

Pleistocene dunes Isla Mujeres, Mexico Whisker crystal cement. This closeup view shows details of orientation and size of these low-Mg calcite Crystals.

X.N.

0.09 iSi.. '

163

Pleistocene dunes Isla Mujeres, Mexico Root-hair cements Interstitial areas are crisscrossed by a network of randomly oriented tubes of calcite which have been precipitated around the root hairs of salt bushes and other plants which colonize these dunes. These reflect meteoric va» dose conditions and could be preserved in the geologic record.

0.09

Up. Mississippian Ste. Genevieve Ls. Indiana An ancient example of an oolitic limestone which, despite probable alteration of the ooids from original aragonite to calcite, has undergone very little cementation. Intergranular pore space is completely preserved except near echinoderm fragments where syntaxial rims have formed. Does this reflect preserved intergranular porosity or has an unstable cement been leached out?

X.N.

0,25 mm

Jurassic-Cretaceous pisoiitic Is. series Italy Ooids (micritized and radially recrystallized) with a coarse fibrous cement fringe (perhaps indicating intertidal or subtidal cementation).

X.N.

0.38

164

Mississippian Coral L s . England Small clam or ostracode showing coarse sparry calcite cavity filling. Fine-grained fringe on inside of shell is followed by very coarse calcite spar. This is a typical voidfilling fabric.

X.N.

0.38 mm

Mississippian part of Lodgepole Ls.. Montana Cloudy, radiaxial fibrous spar filling of a mol lusk-bounded void. The reasons for the unusual optical properties and inclusions in this type of spar are not clear but this type of cement is apparently very early and is common in Mississippian bioherm mounds. It may represent alteration of original submarine aragonite cement.

X.N.

0.38 mm

Up. Silurian Keyser L s . Pennsylvania

part

of

Tonoloway-

Crinoid biosparite with extensive rim cementation of crinoid fragments. Each crinoid grain is surrounded by an optically continuous cementing rim of calcite—such syntaxial overgrowths are generally early diagenetic and often completely destroy porosity in echinoderm-rich sediments.

X.N.

0.38 mm

165

Up. Oligocene Suwannee Ls. Florida Highly porous biosparite. Most grains have a thin fringe of equant calcite. The echinoderm fragments, however, have large, optically continuous overgrowths around them, completely filing the surrounding porosity.

G.P.

0.38

Up. Eocene Ocala Fm. Florida Caicite spar overgrowths on a prismatic-walled mollusk shell. Although overgrowth cementation is most common and most extensive on echinoderm fragments, it also occurs on other grains. It is most clearly recognizable when the substrate crystal structure is coarse and uniform as in this molluscan grain. Outline of original shell wall is visible due to inclusions within the calcite of the shell and traces of original micrite envelope. X.N.

0.38 mm

Up. Triassic Dachstein L s . Austria Fibrous calcite vein with long axes of crystals oriented perpendicular to vein walls. Such textures are often (but not invariably) indicative of void filling.

X.N.

0.38 mm

166 L o . Cretaceous Folkestone beds England

P o i k i l o t o p i c cement. A single c a l c i t e c r y s t a l cements a large number o f d e t r i t a l c l a s t i c grains. Such fab» r i c s are most common in c l a s t i c sediments where a few carbonate grains may act as nuclei for very large cement c r y s t a l s .

X.N.

0.38

L o . P l i o c e n e Tamiami Fm. Florida Small clam w i t h coarse c a l c i t e i n f i l l i n g of central v o i d . Note increasing c r y s t a l size going from shell w a l l to center of cavity—this is common in v o i d f i l l cementation (but not r e s t r i c t e d to i t ) .

X.N.

0.38 mm

L o . P e n n s y l v a n i a n Hale F m . Oklahoma A n example of m u l t i p l e generations of cementation in a carbonate. Bryozoan fragments are encrusted w i t h sparry c a l c i t e v o i d f i l l i n g . The rest of the v o i d space was f i l l e d by a n k e r i t i c dolomite w h i c h is a s s o c i a t e d w i t h an unconformity w h i c h directly overlies this unit, Thus, the t i m i n g of cement formation can sometimes be t i e d into datable geological e v e n t s .

0.25

167

Up. Cretaceous El Abra Ls. Mexico A complex infilling of a large cavity. There is geopetal infiltration of silt which floors part of the cavity (avoiding highs) and alternates with thick and thin layers of sparry calcite (bladed) cement. Final filling is by uniform, equant calcite.

0.64 mm

Pliocene and Pleistocene Caloosahatchee Fm. Florida Partial inversion of a vermetid gastropod shell. Small brown inclusion is unaltered remnant of aragonitic shell while rest has gone to a coarsely crystalline sparry calcite. Virtually no relict texture seen in inverted areas. Also note the extension of calcite crystals into the cavity-filling micrite through displacement or replacement.

0.64 mm

Lo. and Mid. Pennsylvanian Bloyd(?) Fm. Oklahoma A bryozoan biosparite seen under cathodoluminescence, and showing much more complex cementation than would be seen with normal light microscopy. This sediment would show only one generation of cement in polarized light but shows at least 2 generations here. The color differences reflect small variations in trace element composition of the calcite.

Cathodoluminescence

0.30 mm

168 U p . Cretaceous Chalk B r i t i s h North Sea well 4 9 / 2 1 - 3 SEM view of a chalk w h i c h has been buried less than 500 meters deep. Note abundant c o c c o l i t h s and small crystals derived from coccolith breakdown. P o r o s i t y i s over 4 0 percent and c r y s t a l s are rounded and n o n - i n t e r l o c k i n g in t h i s sediment.

SEM Mag. 5000X

2.5 ft m

Up. Cretaceous Chalk B r i t i s h North Sea w e l l 30/16-3 SEM view of a chalk which has been buried in excess of 2000 meters deep. Although o r i g i n a l l y the same type of sediment as the previous chalk, this sediment has undergone extensive pressure solution and rep r e c i p i t a t i o n . P o r o s i t y has been reduced to 15-20 percent, c r y s t a l s are angular, equant, and i n t e r l o c k i n g , y e t c o c c o l i t h remains can s t i l l be seen.

SEM Mag. 10,OO0X

1.3 yum

Up. Cretaceous Chalk Norwegian North Sea w e l l 2/4-2X SEM view of a chalk which has been buried more than 3000 meters deep., T h i s shows the end member of the c y c l e of cementation in chalks* P o r o s i t y has been reduced to less than 10 percent, c r y s t a l s are large, euhedral, and c l o s e l y i n t e r l o c k i n g . Although such cementation is not v i s i b l e in l i g h t microscopy, i t is clearly visible with SEM, and strongly a f f e c t s the reservoir prope r t i e s of fine-grained limestones.

SEM Mag. 10,000X

1.3/im

169

Carbonate Textures Folk Classification Types

This page intentionally left blank.

171

ALLOCHEMICAL ROCKS i

ORTHOCHEMICAL ROCKS m

n

SFARRY CALCITE CEMENT

MICROCRYSTALLINE CALCITE LACKING ALLOCHEMS

MCROCRYSTALLINE CALCITE MATRIX

INTRACLASTS (i)

Z

o o Q.

8

INTRASPARITEtli)

MICRITEtmJ

INTRAMICRITEOi)

Folk's (1962) classification of carbonate rocks

OOLITES (o) DISMICRITEIMnX)

OOWCP.ITE0M

OOSPARITEfU

u UJ

I U

AUTOCHTHONOUS REEF ROCKS

O BIOMICRITECSk)

BIOSPARITECU)

Sparry Calelt*

r.'-.-.'l MlcmtrjilolJIn. Cglclre • . • • : • * : • . » • : : • •

•••:->.r:i>-.::'.-?:-

OVER Percent Altochems

2/3

BIOUTHITEtm

PELMKRITEOf)

PELSPARITEdp)

LIME

MUO

M A T R I X SUBEOUAL OVER 2 / 3 SPAR

0-1 %

Representative MICRITE a

I-10 %

10-50%

FOSSIU-

SPARSE

SORTING OVER 50% LIME MUD POOR POORLY

PACKED

FEROUS

Rock

DISMICRITE MICRITE

Term s

a

SPAR

CEMENT

SORTING ROUNDED 8 ABRADED GOOD

UNSORTED SORTED

ROUNDED

Folk's (1962) classification

WASHED B10MICRITEBI0MICR1TE

BIOSPARITEBIOSPARITEBIOSPARITE BIOSPARITE

S ondy Ctaystone

or Sandstone

of carbonate textures

1959 Terminology Terrigenous Analogues

C I o y • t on •

Clayey Immature

Submoture Sandstone

Mature Supermoture SandstoneSandstone

LIME

MUD MATRIX

SPARRY CALCITE CEMENT

Dunham's (1962) classification of carbonate rocks DEPOSITIONAL

TEXTURE

Originai Components Not Bound Together During Deposition Contains mud ( particles of clay and fine silt size ) Mud-supported Less than 10 percent grains

More than 10 oercent grains

M ud stone

Wackestone

Grain-supported

Pack stone

DEPOSITIONAL TEXTURE NOT RECOGNJZABLE

RECOGNIZABLE

Lacks mud and is grain-supported

G ra i n s l o n e

Original components were bound together during deposition... as shown by intergrown skeletal matter, lamination contrary to gravity, or sediment-floored cavities that are roofed over by organic or questionably organic matter and are too targe to be interstices. Boundstoiife

C r y s t a l 1 ine

Carbonate

( Subdivide according to classifications designed to bear on physical texture or diagenesis.)

Grain-Size Scale for Carbonate Rocks

Transported Constituent!

Authigenic Constituents

V e r y c o a r s e calcirudite 64

mm

16

mm

4

mm

Coarse calcirudite

Extremely coarsely crystalline

Medium calcirudite Fine calcirudite 1

mm

0.5

mm

•4

mm

•1

mm

' 0.25

mm

Very c o a r s e l y crystalline

Coarse calcarenite C o a r s e l y crystalline Medium calcarenite 0.25

mm Fine c a l c a r e n i t e

0 . 1 2 5 mm.

Medium c r y s t a l l i n e V e r y fine c a l c a r e n i t e

0.062 mm

'0.062 mm C o a r s e calcilutite

0.031 m m

Finely crystalline Medium calcilutite

0 . 0 1 6 mm

•0.016 m m Fine calcilutite

0.008 mm 0. 004 mm

Very finely c r y s t a l l i n e Very fine calcilutite

•0.004 mm Aphanocrystalline

Carbonate rocks contain both physically transported particles (oolites, intraclasts, fossils, and pellets) and chemically precipitated minerals (either as pore-filling cement, primary ooze, or as products of recrystallization and replacement). Therefore the size scale must be a double one, so that one can distinguish which constituent is being considered (e.g. calcirudites may be cemented with very finely crystalline dolomite, and finer calcarenites may be cemented with coarsely crystalline calcite), The size scale for transported constituents uses the terms of Grabau but retains the finer divisions of Wentworth except in the calcirudite range; for dolomites of obviously allochemical origin, the terms dolorudite, doloarenite, and dololutite are substituted for those shown. The most common crystal size for dolomite appears to be between .062 and .25 mm, and for this reason that interval was chosen as the medium crystalline class (from Folk, 1962).

Ion Strength, Environment, and Carbonate Morphology (from Folk, 1974) Environment

Chemistry

Crystal habit

Mg High

Na

High

Hypersaline to Normal Marine, Beachrock, Sabkha, Submerged Reefs, etc.

Steep rhombs of Mg-Calcite with vertically-oriented flutings; Fibers of Mg-Calcite and Aragonite; growth rapid in c-direction; very slow laterally because of selective Mg-poisoning. Crystals limited in width to a few microns.

(Mg Low)

Na

High

Mainly connate subsurface waters

Complex polyhedra and anhedra of calcite; lack of M g allows unhampered growth and equant habit.

( M g Low)

Na moderate to low

Meteoric phreatic, to deep subsurface mingling between meteoric and connate water

Complex polyhedra and anhedra of calcite; lack of M g and slow crystallization allows equant crystals, often coarse.

(Mg Low)

(Na Low)

Meteoric vadose; caliche; streams and lakes

Simple unit rhombohedra of calcite

(Mg Low)

(Na Low)

Streams, Lakes,

Calcite micrite. Also, calcite sheets or hexagonal crystals with basal pinacoids; sheet-structure on edges visible due to very rapid lateral growth in the absence of Mg-poisoning.

Caliche

173 Mid. Ordovicion Chazy and Black River Ls, Pennsylvania Intrasparite with sparsely fossiliferous micrite clasts. (Grainstone)..

X.N.

0.38 mm

Paleozoic Is. U°S„ Midcontinent Oosparite with coated fossil fragments. (Grainstone).

X.N.

0.30 mm

Up. Oligocene Suwannee Ls. Florida Biosparite with echinoderms, mi I iolid Foratninifera, mollusks, etc. (Grainstone).

X.N.

0.38 mm

174

Paleozoic (fm?) Alabama Pelsparite. (Grainstone).

0.38 mm

Up- Permian Capitan Ls. New Mexico Intramicrite with pelsparite clasts in a largely micritic matrix. Parts of this rock could be classified as a poorly-washed irttrasparite. (Packstone).

0.38 mm

Lo. Ordovician Beekmantown L s . Maryland Oomicrite (oolites have been strongly deformed). (Packstone).

0.38 mm

175 Pliocene and P l e i s t o c e n e Caloosahatchee Marl Florida B i o m i c r i t e w i t h mainly pelecypod fragments, (Wackestone),

P.X.N.

0.38

J u r a s s i c Solnhofen L s . (Kelheim facies) Germany P e l m i c r i t e (really a b i o p e i m i c r i t e because of abundant f o s s i l fragments mixed w i t h the p e l l e t grains). (Wackestone or packstone).

0.38 mm

J u r a s s i c Solnhofen L s . (Kelheim facies) Germany M i c r i t e (rather pure l i t h i f i e d carbonate mud). (Mudstone).

X.N.

••MRS!.

-"w\v

••.::,.>•-;

«sflwiia***s

mmwm

0.38 mm

176

Pleistocene Key Largo L s . Florida Red algal b i o l i t h i t c In situ encrustation of red algae on corals and other grains, (Boundstone),

X.N.

0.38 mm

Mid. Ordovician Bays and Athens L s . equivalent Virginia Dismicrite (really a dispelmicrite). Large void {not a solution vug) disrupting normal sediment textureorigin unknown.

X.N.

0.38 mm

Lo. Ordovician Stonehenge Ls. Pennsylvania Coarse replacement dolomite.

X.N.

0.38 mm

177

Eocene Oberaudorf Schichten Austria A calclithite. More than 50 percent composed of detrital carbonate clasts (reworked, older-cycle limestones and dolomites). Often polymict, these deposits are generally important only on the downthrown sides of major faults or in extremely arid areas.

X.N.

0.64 mm

Up. Jurassic Calpionellid Ls, Italy This photograph, and the six that follow, illustrate the spectrum of carbonate rock textures as classified by Folk (1962). Dunham (1962) classifications given in parenthesis. Fossiliferous micrite. Fossils are very fine-grained and include pelagic Foraminifera, calpionellids, and spicules. (Mudstone).

X.N.

0.38 mm

Up. Cretaceous Greenhorn L s . Colorado Sparse biomicrite (mainly pelagic Foraminifera). (Wackestone).

X.N.

0.30 mm

178

Lo. Pliocene Tamiami Fm. Florida Packed biomicrite. (Peneroplid Foraminifera and quartz sand grains.) (Packstone).

X.N.

0.38 mm

Pliocene and Pleistocene Caloosahatchee Marl Florida Poorly washed biosparite containing molluscan and algal fragments. (Packstone).

0.38

Mid. Ordovician fm.(?) Virginia Poorly sorted (unsorted) intrasparite. (Grainstone).

X.N.

0.24 mm

179 Holocene sediment Cat Cay, Bahamas Rounded (and (Grainstone).

X.N.

w-A

J0M •v

•ft

sorted)

oosparite.

0.38 mm

Mississippian Waulsortian Ls. Ireland This is a grain supported fabric which illustrates the difficulty of determining grain packing. These grains of fenestrate bryozoans are irregular in shape and, when uncemented, have as much as 90 percent porosity. If pore space were infiltrated with mud one might incorrectly class this as a mudsupported fabric.

1.24 mm

Burrows and Borings

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183 Holocene sediment Schooner C a y s , Bahamas Example of modern subtidal boring of carbonate g r a i n s . Many organisms produce borings but sponges, algae and fungi are among the most important. Here much o f the grain structure of the o o i d has been destroyed by boring, p o s s i b l y l a r g e l y by a l g a e .

0.05

Is

H o l o c e n e sediment B i m i n i , Bahamas A strongly bored mollusk fragment. Numerous small a l g a l and fungal tubes have cut the c r o s s e d - l a m e l l a r structure of t h i s grain. R e c o g n i t i o n of a l g a l borings is important in that i t is e v i d e n c e that the grain was derived from the photic zone. The borings of c l i o n i d sponges, a c r o t h o racican barnacles, and ctenostome bryozoa could a l l be mistaken for algal borings unless c a r e f u l l y examined.

.J*£fe

0.09 mm

I

i

Holocene sediment B e l i z e ( B r i t i s h Honduras) SEM v i e w of an algal tubule w i t h i n a coral s k e l e t o n . A l g a l photosynt h e t i c a c t i v i t i e s can lead to the prec i p i t a t i o n of a sheath of carbonate (generally aragonite or high-Mg c a l c i t e ) around the f i l a m e n t s ; these are common in SEM v i e w s of modern sediments. A g a i n , recognition of algal tubules a l l o w s determination of an environment w i t h i n the photic zone.

SEM Mag. 3000X

4.1 /xm

184

Up. Cretaceous White Ls. Northern Ireland A sponge boring within a belemnite rostrum. Sponge borings are distinguished by their relatively large size and characteristic shape. The silt-sized debris from the borings of some modern sponges adds a significant fraction to the internal sediment within reefs and fore-reefs. Sponge bioerosion is also important in the destruction of carbonate shorelines.

0.22 mm >

Up. Cretaceous White Ls Northern Ireland Multiple sponge borings within a belemnite rostrum. Note that the area within the borings has been infilled with the same type of micritic sediment that is found in the rest of the sediment. Yet the area within the borings has been protected from compaction and thus shows the original sediment fabric while the external areas show pervasive bedding-parallel compaction and grain crushing.

0.25 mm

Mid. Jurassic lower Forest Marble beds England A boring. Borings and burrows must be carefully distinguished. Borings occur in hard substrates; burrows in soft ones. The truncation of shells by this structure indicates that the sediment must have been significantly lithified at the time of boring. Burrows normally would pass around such grains in soft sediment. Thus, one can determine presence or absence of early Iithification.

0.64 mm

185

Mid. Ordovician Bays L s . Virginia A sand-filled burrow in siity carbonate mudstone. Burrows are often detected by gross or subtle changes in texture as coarser or finer sediments are brought in by the burrowing organism. This burrow has been compacted during later diagenesis (although oblique sections w i l l also give elliptical shape).

0.25 mm

Up. Cretaceous Monte Antolo Fm. Italy These slightly compacted burrows are part of a single burrow system probably produced by Chondrites. Note that they have a consistent orientation with respect to each other. Burrows can be filled with pyrite, calcite, glauconite, and other diagenetic phases, as well as with primary sediment.

0.64 mm

187

Crusts and Coatings

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189 Lo. Eocene Indian Meadows Fm. Wyoming Part of a blue-green algal oncolite.. Well, but irregularly laminated, large (about 2 cm across) grains of probable algal origin. Insoluble residues of thin sections of these grains w i l l often still show algal tubules or filaments.

0.30 mm

Quaternary caliche crust Texas Irregularly laminated caliche crust trapping carbonate and non-carbonate grains. Such crusts (which must be distinguished from algal structures) can indicate unconformities and subaerial exposure in carbonate sections. Inverse grading, autofracturing, interlocking grains, and microstalactitic textures (not shown here) aid in identification.

0.38 mm

Holocene beachrock Bahamas Beachrock (with cementing crust of small fibrous aragonite needles) contains numerous "grapestone" grains (composite grains held together loosely and, here, secondarily oolitically coated before cementation). Illustrates encrustation (oolitic coatings and cement crusts).

X.N.

0.38 mm

190

Cretaceous Tama bra l_s. Mexico Isolated encrustations of grains can be produced by algae (as here), Foraminifera, bryozoans, and other organisms. Such encrustations can be extremely important in l i t h i f i cation of sediment within the environment of deposition. Such biolithites are, however, often difficult to recognize because of the vague nature of many algal products and because of later diagenesis.

0.51 mm

Pleistocene aeolianite Abu Dhabi Micrite envelopes must be distinguished from encrustations. In most cases, micrite envelopes are thin zones of surficial alteration (boring) of grains which micritizes their outer surface. Thus, there is no addition of material to the exterior of a grain. As seen here, micrite envelopes can remain even after grains are leached away.

0.09 mm

Mid. Jurassic lower Forest Marble beds England An example of ancient micrite envelopes and subordinate encrustations. Thin rinds of micrite can be seen with occasional irregular protrusions toward the former grain interiors—these are formed by microboring. Occasional bulges of thicker micrite are encrustations. The micrite envelopes have acted as a template for cementation of both internal (leached) and external porosity.

0.64 mm

191

Dissolution Fabrics

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193

Up. Cretaceous Pilot Knob reef fades of Austin Group Texas Leached grains with micrite envelopes. Most grains show no internal structure and a single dark micritic rim. This is produced by algal boring of original aragonitic skeletal grains (producing dark envelopes) and subsequent dissolution of the unstable aragonite.

0.38 mm

Up. Cretaceous Pilot Knob reef facies of Austin Group Texas Large mollusk grain which originally had two-layer structure (one aragonite, one calcite). Calcific layer preserved while the aragonitic layer was dissolved and replaced by sparry calcite. Note micrite envelope defining former aragonitic zone.

X.N.

0.30 mm

Up. Cretaceous El Abra Ls„ Mexico The odd texture, shown here, of miliolids essentially " f l o a t i n g " in sparry calcite is the product of dissolution of the aragonitic shell layer of a Toucasia rudistid. The calcific wall layer is still preserved in brownish original material while the aragonitic layer was leached after partial cementation of the matrix sediment; The leach void was later filled with clear, sparry calcite.

0.64 mm

194

Pleistocene aeolianite Abu Dhabi Fossils, especially originally aragonitic ones, can be leached, leaving a series of unfilled micrite envelopes. In this example, several freestanding micrite envelopes are acting as a template for the internal and external cementation by sparry lowMg calcite cement. If continued, this process will yield fabrics such as those seen in the previous three photos.

m: X.N.

0.07 mm •

Mid. Eocene Avon Park Ls. Florida Leached fossils in a dolomitic rock. Either the matrix was dolomitized and the fossils leached, or fossils were leached and rock matrix was then dolomitized (dolomite apparently replaces more readily than it cements). Thus, determining the paragenetic sequence in such rocks can be very difficult.

G.P.

0.38 mm

Jurassic Is. of Ronda unit (Subbetic) Spain Selective leaching of dolomite (dedolomitization) has taken place in this rock. This is a common nearsurface process and is aided by the presence of evaporites (sulphate minerals).

X.N.

0.38 mm

r

'

* • • • • •

-

•

A

t

195 Cretaceous Tamabra L s . Mexico

O c c a s i o n a l l y the t i m i n g of leaching can be c l o s e l y d a t e d . Here, in the lower center of the photo, one can see sediment i n f i l l i n g a f o s s i l . T h i s c l e a r l y implies very early d i s s o l u tion of the f o s s i l (probably vadose diagenesis) and i n f i l l i n g w i t h internal sediment or vadose s i l t .

0.64 mm

197

Replacement and Neomorphism

198 (d agram after F o l k , 1965}

CALCITE

REPLACEMENT

OR

INVERSION ARAGONITE MUD OR OR SKELETON-* CALCITE MOSAIC TRANSFORMATION

PLACED BY ITS POLYMORPH

ALLOTROPIC RECRYSTALLIZATION

NOT SPECIFIED

A DZFORMED MINERAL CHANGES TO A

STRAINED CALCITE — UNSTRAINED CALCITE

MOSAIC OF UNDEFORMEO CRYSTALS Or THE SAME M I N -

RECRYSTALLIZATION

(STRAIN) RECRYSTAL-

RECRYSTALLIZATION

LIZATION

ERAL

AN UNOEFORMED MINERAL CHANGES TS FORM, GRAIN SIZE OR ORIENTATION

A MINERAL SOLVES

DIS-

LEAVING A

CAVITY, CAVITY FILLED

LATER

IS

CALCITE MUD OR FIBERS — CALCITE MOSAIC, ETC.

RECRYSTALLIZATION

SKELETON — CAVITY-* CALCITE

RARE NO SPECIAL TERM

GRAIN GROWTH

GRAIN GROWTH (OR GRAIN DIMINUTION)

NO SPECIAL TERM

Comparison of terminology for mineral alterations as observed with petrographic microscope, observe particularly the varying status of the term recrystallization. It is proposed that grain

INVERSION

JTRAIN RECRYSTALLIZATION

RECRYSTALLIZATICN (AND DEGRADING RECRYSTALLIZATION)

SOLUTION-CAVITY FILL

growth not be used for sedimentary carbonate rocks, because the process of grain growth in metals does not resemble any diagenetic process in normal limestones.

A Code for Directly Precipitated Calcite Formative Mechanism

Foundation

Syntaxial Overgrowth (0)

Directly Precipitated (P)

Crusts-(C)oriented physically on surface

Randomlyoriented

USAGE

METASOMATISM

PYRITE, ETC

A MINERAL IS R E -

STRICT

(after Folk, 1965)

Grain Shape

Term

Symbol

Terms of Bathurst (1958)

Equant; on monocrystalline nucleus

x-Monocrystalline 1 Overgrowth

P.E*O m

Rim-Cement

Equant; on polycrystalline nucleus

x-Equant Overgrowth

P,E*0

Bladed-on polycrystalline nucleus

x-Bladed Overgrowth

P.B'O

Fibrous-on polycrystalline nucleus

x-Fibrous Overgrowth

P.F*0

Equant

x-Equant Crust

P.E*C(W)

Bladed

x-Bladed Crust

PB*C (W ,

Fibrous

x-Fibrous Crust

P.F*C,„,

Equant

x-Mosair

P.E*

Bladed

Very rare or non-existent "Bladed Mosaic" may perhaps exist; "Fibrous Mosaic" probably non-existent.

Fibrous

N E O M O R P H I S M

OF A DIFFERENT COMPOSITION

THIS PAPER

REPLACEMENT

DOLOMITE,

( L O O S E L Y )

ANOTHER

BATHURST (I958) VOLL096O) ETC LOOSE[

^CRYSTALLIZATION (LOOSELYT\

MINERAL RE -

TERM

IGNEOUS TERM

REPLACEMENT

ONE

PLACES

METAMORPHIC OR METALLURGICAL

EXAMPLE

PROCESS

Drusy Mosaic (inside fossils, etc.)

Granular Cement (if between allochems)

i

* Add number for crystal size, e.g. P.E,O m , P.F»C. x Add crystal sire term, e.g. Finely Bladed overgrowth (or finely crystalline Bladed overgrowth); Medium Fibrous crust (medium crystalline Fibrous crust). 1 Monocrvstals mav be Bladed or rarely Fibrous; use "Bladed Monocrystalline overgrowth" if desired, P.BOm, etc. '

199 U p . Cambrian Mines Dolomite Mbr. of Gatesburg F m . Pennsylvania Replacement, O r i g i n a l o o l i t i c limestone has been completely replaced by quartz in the form of chert, c h a l cedony, and mega-quartz. Although t h i s example shows remarkable preservation of o r i g i n a l d e t a i l , many replacement textures simply obliterate o r i g i n a l f a b r i c s .

X.N.

0.38 mm

U p . Cambrian K i f t a t i n n y L s . New Jersey Dolomite replacement w i t h retention of r e l i c t or " g h o s t " t e x t u r e . O r i g i nal sediment was a porous o o l i t e , probably later spar cemented, and f i n a l l y completely replaced by dolom i t e . Ooids can be recognized because organic matter and other impurities have been retained in the dolomite replacement.

0.38 mm
P l i o c e n e and P l e i s t o c e n e Caloosahatchee F m . Florida

* t

Inversion. Originally aragonitic shell of a vemetid gastropod i s here partly inverted to c a l c i t e . The coarse spar is c a l c i t e and the darker patches are s t i l l aragonite. Note total loss of primary texture w i t h i n the inverted areas and the partial overlap of the c r y s t a l s (by displacement or inversion} into m i c r i t i c matrix.

0,64 mm

200 M i d . O r d o v i c i a n Chazy and Black River l_s. Pennsylvania Recrystal l i z a t i o n of micrite to microspar and pseudospar (see F o l k , 1965). V i r t u a l l y complete diagenetic a l t e r a t i o n o f primary texture.

0.38 mm

M i d . O r d o v i c i a n Chazy and Black River L s . Pennsylvania Recrystal l i z a t i o n of micrite to microspar and pseudospar. Note irregular grain shapes of pseudospar c r y s t a l s . Complete diagenetic a l teration of primary depositional texture.

0.38

Up. Cretaceous Monte A n t o l a Fm. Italy Strain r e c r y s t a l l i z a t i o n . These veins are thin zones of microspar which have formed along v i r t u a l l y i n v i s i b l e microfractures or zones of shear. A l t h o u g h Hi ese veins can grow to look very s i m i l a r to fracture v e i n s , there never was any open v o i d space a s s o c i a t e d w i t h these, as evidenced by f o s s i l s and other grains going across them w i t h o u t breakage.

0.11 mm

201

Jurassic(?) Carrara Marbie Italy The end product of extensive strain recrystallization. The entire rock has gone to a uniform mosaic of medium-crystalline, equant crystals with rather straight intercrystalline boundaries. The driving mechanisms were temperature as well as stress during metamorphism. This unusually uniform marble is used for sculpture and building stone.

X.N.

0.64 mm

Paieocene (Danian) Faxekalk Denmark Solution-cavity f i l l . This originally aragonitic skeleton of a coral (Dendrophyllia candelabra) has been altered to calcite by going through a phase of complete dissolution and later infilling of the leached void. This has led to complete obliteration of the internal wall structure of the coral; only skeletal outline remains.

0.40 mm

Up. Mississippian Hindsville Ls. Oklahoma Solution-cavity f i l l A pelecypod shell with two-layer structure has undergone alteration from aragonite to calcite by either solution-cavity f i l l or inversion. Original shell structure has been largely obliterated and coarse, sparry calcite now fills shell. Distinguishing between solutioncavity fill and inversion can be impossible in many cases.

0.19 mm

203

Compaction and Deformation

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205 Cretaceous Gmunden F l y s c h Austria E x c e l l e n t orientation of grains (esp e c i a l l y sponge s p i c u l e s ) . T h i s is produced, in part, by primary sedimentary processess but is greatly enhanced by compaction w h i c h produces something akin to f i s s i l i t y by grain rotation into bedding-plane parallelism. Although compaction has not yet been w i d e l y recognized in s h a l l o w - w a t e r carbonates, it i s common in deeper-water carbonates.

X.N.

0.38 mm

Up. Cretaceous White L s . Northern Ireland Intense, bedding-parallel compaction and crushing of t h i n - w a l l e d organisms in a c h a l k . Such compaction is e s p e c i a l l y common in areas where there has been extremely rapid loading of overburden. In t h i s area, t h i c k basalt f l o w s o v e r l i e the c h a l k .

0.11 mm

L o . Cretaceous Edwards L s . Texas Shattered m i c r i t e envelopes are an i n d i c a t o r of compaction or deformation of the sediment before major cementation. Because of the f r a g i l e nature of these envelopes, however, i t does not take much compaction to destroy them.

0.25 mm

206 Mid. Ordovician Black River(?) L s . Pennsylvania Stylolite solution zone. Dark lines are solution interfaces with concentration of insoluble minerals (especially clays and iron minerals). Dolomite is abundant along these stylolites. Stylolites are often associated with strong deformation or compaction and provide late diagenetic cement for many units.

0.38 mm

Lo. and Mid. Pennsylvanian Marble

Falls Ls. Texas Solution zone marked by stylolitic insoluble residue shown cutting a crinoid fragment. Loss of a large volume of carbonate is apparent from the truncation of the crinoid.

X.N.

0,38 mm

Lo. Devonian Becraft Ls. New York Extreme case of stylolitization in which a large brachiopod shell and numerous echinoderm fragments (with syntaxial overgrowths) have mutually dissolved and interpenetrated each other.

0.38

207 Up. M i s s i s s i p p i a n Ste. Genevieve l_s, Tennessee An i n t e r e s t i n g example of compaction postdating cementation. Although ooids show e x t e n s i v e grain interpenetration there are v i r t u a l l y no grain-to-grain c o n t a c t s . In each case, a cement rim intervenes. T h u s , thin rinds of submarine cement must have formed early in the history and compaction and grain interpenetration followed later.

X.N.

0.38

Up. Cambrian Gatesburg Fm. Pennsylvania Moderately deformed o o i d showing how concentric laminations are sheared from the n u c l e u s . Such textures may i n d i c a t e that cementat i o n was late r e l a t i v e to deformation.

X.N.

0.30

Up. Cambrian Gatesburg Fm, Pennsylvania Strongly deformed ooids (spasroliths) showing how strong compression w i l l shear off outer concentric coatings of the ooids and produce shapes often d i f f i c u l t to i d e n t i f y as o o i d s .

X.N.

0.38

208 Lower Jurassic Hierlatzkalk Germany

M u l t i p l e fractures (now f i l l e d with sparry c a l c i t e ) c u t t i n g a sparse biom i c r i t e . T h i s rock comes from a thrust s l i c e in the northern A l p s ,

m

0.38 mm

Up. Cretaceous Chalk England A strongly fractured chalk from an area of only m i l d deformation. Such fractures are commonly late d i a genetic, and postdate most other diagenetic features in the rock. They can o c c a s i o n a l l y be used to predict the o r i e n t a t i o n and proximity of fault zones.

0.40 mm

J u r a s s i c Pennine Bu'ndnerschiefer Switzerland Extreme deformation and a l t e r a t i o n o f an impure limestone. Crenulate f o l d i n g , development of new micas, and strain r e c r y s t a l l i z a t i o n of c a l c i t e are a l l present.

X.N.

0.64 mm

209

Geopetal Fabrics

This page intentionally left blank.

^m

211 Up. M i s s i s s i p p i a n H i n d s v i l l e L s . Oklahoma

Geopetal sediment i n f i l l i n g of a pelecypod s h e l l . Note the a l t e r a t i o n of the shell w a l l w i t h o u t the d i s placement of the sediment f i l l i n g — this implies i n v e r s i o n rather than complete d i s s o l u t i o n and subsequent void f i l l . Not a l l geopetal f i l l s are exactly h o r i z o n t a l so a s t a t i s t i c a l sampling should be used.

P.X.N.

0,20

P l i o c e n e and P l e i s t o c e n e Caloosahatchee Marl

Florida Geopetal filling of a gastropod chamber,. Mud (micrite) f i l l s the lower part of the c a v i t y w h i l e sparry c a l c i t e f i l l s the upper part—the contact i n d i c a t e s an approximately level surface at the time of d e p o s i t i o n . Such structures are very useful in determining original dips of u n i t s .

0.38

Up. Cambrian A l l e n t o w n Dolomite Pennsylvania Geopetal o o i d s . O r i g i n a l circular o u t l i n e of ooids can be seen. D i s solution of part of the ooids a l l o w e d the remainder to fall to bottom of c a v i t y . Upper part then f i l l e d w i t h spar. Indicates level surface at time of d i s s o l u t i o n .

0.38 mm

212 Up. Cambrian Morgan Creek L s . Mbr. of Wilberns Fm. Texas " U m b r e l l a " v o i d . Presence of the large f o s s i l fragments prevented the complete i n f i l t r a t i o n of lime mud and maintained shelter voids which were later f i l l e d w i t h sparry c a l c i t e . This can be used as a geopetal indicator.

0.38 mm

Pliocene and Pleistocene Caloosahatchee Marl Florida Umbrella void—large mo husk fragment prevented i n f i l t r a t i o n of micrite and maintained c a v i t y f i l l e d by later crust of bladed spar and equant spar. 0.38 mm

Cretaceous Tamabra |_s. Mexico Geopetal sediment or vadose-silt i n f i l l i n g of voids of f o s s i l s (aragon i t i c ) which were leached. These geopetal features may reflect postdepositional but prediagenetic structural or compactional deformation, and must thus be d i s t i n g u i s h e d from synsedimentary ones. 0.64 mm

213

Porosity Classification

This page intentionally left blank.

Philip W. Choquette and Lloyd C. Pray BASIC FABRIC

POROSITY

TYPES

SELECTIVE

NOT

INTERPARTICLE

St 1 —

WP

INTERCRYSTAL

8C

MOLOIC

MO

FENESTRAL

FE

SHELTER

SH

GROWTH-

FABRIC

^

D

CH

VUG*

VUG

CAVERN*

CV

OR NOT

BURROW BU

BO

TT

SHRINKAGE SK

TERMS

MODIFIERS

SIZE*

DIRECTION OR STAGE

PROCESS

CHANNEL*

*Cavern applies to man sized or lorger pores of channel or vug shapes

SELECTIVE

MODIFYING GENETIC

FR

3

BORING %

FRACTURE

s

GF

FRAMEWORK

; #

SELECTIVE

BP

INTRAPARTICLE

BRECCIA 8R

FABRIC

MODIFIERS

CLASSES

mm' Img

large SOLUTION

ENLARGED

MEGAPORE

mg

—32smg — 4— Ims

small CEMENTATION

REOUCED

INTERNAL SEDIMENT

FILLED

large MESOPORE

ms

MICROPORE

mc

-256-

-'/2-

smoll

-1/16TIME

OF

FORMATION

PRIMARY

Use size prefixes with basic porosity types: mesovug msVUG small mesomold smsMO microinterporticle mcBP

P

pre-deposilionol

Pp

depositionol

Pd

SECONOARY

*For regular-shaped pores smoller Ihon cavern size.

S

eogenetic

Se

mesogenetic

Sm

telogenetic

SI

r

Genetic modifiers ore combined as follows: PROCESS

+

DIRECTION

•

TIME

Meosures refer lo overage pore diameter of a single pore or the ronge in size of a pore oisembloge. For tubular pores use average cross-section. For ploty pores use width and note shape.

ABUNDANCE

MODIFIERS

percent porosity

(15%) or

EXAMPLES:

solution -enlarged

s«

cement - reduced primary

crP

sediment-filled eogenetic

ifSe

ratio of porosity types

(12)

or ratio and percent

Classification o f Porosity Types (Choquette and Pray, 1 9 7 0 )

( 1 2 ) (15%)

216

TIME-POROSITY TERMS

reef, f r o m e ^ mean high tide up to o few meters

[•_!' ••'^'™ff r-f-qp.-.C-IWB

£tE*E5 I I

.

I

EOGENETIC\

MES06E NETIC ZONE

EOGENETIC

< B Z \

OS

ZONE'

FORMER SIIBAERIAL TELOGENETIC ZONE'

Time-porosity terms and zones of creation and modification of porosity in sedimentary carbonates. Upper diagram: Interrelation of major timeporosity terms. Primary porosity either originates at time of deposition (depositional porosity) or was present in particles before their final deposition (predepositional porosity). Secondary or postdepositional porosity originates after final deposition and is subdivided into eogenetic, mesogenetic, or telogenetic porosity depending on stage or burial zone in which it develops (see lower diagram). Bar diagram depicts our concept of " t y p i c a l " relative durations of stages. Lower diagram: Schematic representation of major surface and burial zones in which porosi-

ty is created or modified. Two major surface realms are those of net deposition and net erosion. Upper cross section and enlarged diagrams A, B, and C depict three major postdepositional zones. Eogenetic zone extends from surface of newly deposited carbonate to depths where processes genetically related to surface become ineffective. Telogenetic zone extends from erosion surface to depths at which major surface-related erosional processes become ineffective. Below a subaerial erosion surface, practical lower limit of telogenesis is at or near water table. Mesogenetic zone lies below major influences of processes operating at surface. The three terms also apply to time, processes, or features developed in respective zones. (from Choquette & Pray, 1970)

217

Holocene oolite Great Salt Lake, Utah Unfilled interparticle porosity (in oolite). Porosity in black. Classification used in these and following photos is that of Choquette and Pray (1970).

X.N.

0.30 mm

Up. Mississippian Pitkin Ls. Oklahoma Sparry calcite-filled porosity (in oolite).

X.N.

interparticle

0,10 mm

Up. Eocene Ocala Fm. Florida Enlarged intergranular (interparticle) porosity (probably enlarged through solution). Porosity in black. Grains are mostly miiiolid Foraminifera.

X.N.

0.38 mm

218

Holocene back-reef beach sediment Belize (British Honduras) Unfilled intraparticle porosity (within a large coral fragment). Porosity in black.

X.N.

0.38 mm

*

Pleistocene Key Largo Ls, Florida

0 *1>

Reduced interparticle and intraparticle porosity (in Foraminifera and mollusks). Porosity in black.

-|E.

>**

t Jim t V / ' ^ r « -

X.N.

0.38

Up Oligocene Suwannee Fm. Florida Reduced intraparticle porosity (especially within miliolid Foraminifera) and reduced interparticle porosity (especially adjacent to echinoid fragments). Porosity in purple.

G.P.

0.38 mm

j

?

i„

219

Up. Eocene Ocala Fm. Florida Reduced intraparticle (within miliolid Foraminifera) and interparticle porosity. Cement here is chert. Porosity in black.

X.N.

0.38

Mid. Eocene Avon Park L s . Florida Intercrystal porosity in a fine- to medium-crystalline dolomite (replacement). Porosity in black (with strain patterns).

X.N.

0.38

Pleistocene Miami oolite Florida Moldic (oomoldic) porosity (black).

X.N.

0.38 mm

220 Up- Eocene Ocala L s . Florida

Moldic p o r o s i t y . Formerly a f o s s i l iferous m i c r i t e , the m i c r i t e has been replaced by dolomite and the more soluble c a l c i t i c f o s s i l s have been d i s s o l v e d to leave a moldic p o r o s i t y . P o r o s i t y in purple.

G.P.

0.38 mm

Up. Eocene Ocala L s . Florida Moldic porosity* As above, dolomite replaced the m i c r i t e matrix, then a l l o w e d d i s s o l u t i o n of more soluble f o s s i l s to y i e l d moldic p o r o s i t y . P o r o s i t y in purple.

G.P.

0.38 mm

U p . Cretaceous P i l o t Knob reef facies of A u s t i n Group Texas F i l l e d moldic p o r o s i t y . Rock was cemented by c a l c i t e , then a r a g o n i t i c fossils were dissolved, leaving voids. Subsequently these voids were f i l l e d w i t h sparry c a l c i t e . Former f o s s i l s marked by m i c r i t e envelopes.

0.30 mm

221

Jurassic L s . of Ronda unit (Subbetic) Spain Moldic porosity produced by selective leaching of dolomite crystals (dedolomitization). This is probably a telogenetic (outcrop) process which is enhanced by the presence of evaporite (sulphate) minerals in the section.

X.N.

0.38 mm

Up. Silurian part of TonolowayKeyser Ls. Pennsylvania Filled fenestral porosity in a bluegreen algal biolithite. Porosity may be due to air spaces in crinkled mat sediments.

0.38

•*""BSSW*

Pliocene and Pleistocene Caioosahatchee Marl

Florida Filled shelter porosity large mollusk fragment.

0.38 mm

beneath a

222 Up. Jurassic Solnhofen L s . (Kelheim facies) Germany Reduced fracture porosity. Porosity in black.

X.N.

0.38

Mid. Ordovician Black River(?) L s . Pennsylvania Filled fracture porosity. Conjugate set of large fracture veins.

0.38 mm

Holocene soil crust Florida Secondary enlarged porosity yielding small solution vugs. Porosity in purple. Dark grain in upper left-hand corner is a wood fragment.

G.P.

0.38 mm

223 U p . Oligocene Suwannee L s . Florida Enlarged moldic p o r o s i t y . Note large pelecypod mold with upper edge enlarged. P o r o s i t y in b l a c k . Other grains include mainly m i l i o l i d Foraminifera.

X.N.

0.38 mm

U p . Eocene Ocala Fm. Florida Vuggy p o r o s i t y . Probably solution enlarged. P o r o s i t y in black. Grains include m i l i o l i d s and other Foraminifera.

X.N.

0.38 mm

Up. Cretaceous P i l o t Knob reef facies of A u s t i n Group Texas Vuggy p o r o s i t y , c l e a r l y enlarged and not fabric s e l e c t i v e . P o r o s i t y in black.

X.N.

0.38 mm

224

Pleistocene Key Largo Ls. Florida Vuggy porosity. Probably solution enlargement of original interparticle porosity. Porosity in black.

X.N.

0.38

?

I

,

Techniques

Although petrography is an extremely valuable tool for the identification of minerals and their textural interrelationships, it is best used (in many cases) in conjunction with other techniques. Precise mineral determinations are often aided by staining of thin sections or rock slabs, by X-ray analysis, or by microprobe examination. Where noncarbonate constituents are present in carbonate rocks they often are better analyzed in acid-insoluble residues than in thin section. Where detailed understanding of the trace element chemistry of the sediments is essential. X-ray fluorescence, microprobe, atomic absorption, or cathodoluminescence techniques may be applicable. Commonly, also, sediments may be too fine-grained for adequate examination with the light microscope. The practical limit of resolution of the best light microscopes is in the one to two micrometer {(im) range. Many carbonate and noncarbonate grains fall within or below this size range. Furthermore, because most standard thin sections are about 30 jum thick, a researcher examines 10 or 20 of these small grains stacked on top of one another, with obvious loss of resolution. Smear mounts or strew mounts (slides with individual, disaggregated grains smeared or settled out onto the slide surface) are an aid in examining small grains where the material can be disaggregated into individual components. However, in most cases, scanning and transmission electron microscopy have proved to be the most effective techniques for the detailed

examination of fine-grained sediments. The bibliography of this book provides a number of references to techniques useful in supplementing standard petrographic analysis. Although many of the techniques require sophisticated and expensive equipment, others, such as staining, acetate peels, and insoluble residues can be performed in any laboratory. Because of the potential desirability of these techniques, it is often useful to prepare epoxy-cemented thin sections without coverslips. These sections can be examined under a light microscope either by placing a drop of water and a coverslip on the sample during viewing, or by using mineral oil or index of refraction oils with or without coverslips. These methods involve some loss of resolution but do allow the cleaning and drying of the surface of the section and subsequent staining, luminescence, or microprobe examination. One can even partially or completely immerse the thin section in acetic or hydrochloric acid and decalcify the section thereby sometimes enhancing organic structures or insoluble-mineral fabrics. Finally, uncovered thin sections can also be gound thinner in cases where examination of very fine-grained sediments is needed. Clearly, one can spend a lifetime analyzing a single sample using all possible techniques. Efficient study requires a thorough understanding of all available tools and proper application of the most useful and productive of these.

Staining Staining techniques are among the fastest, simplest, and cheapest methods for getting reliable chemical data on carbonate phases. The following list of minerals and their diagnostic stains is derived from the work of Friedman (1959), Dickson (1966), Milliman (1974), and others. The original papers, listed in the bibliography, will provide details about the exact application and methods. Aragonite Distinguished from calcite by use of Feigel's Solution. Aragonite turns black whereas calcite remains colorless for some time. Mixing Feigel's Solution requires 7.1 g of MnS04. H 2 0 ; 2 to 3 g of Ag2S04; 100 cc distilled water and a 1% NaOH solution. Difficult to prepare and store. Calcite Can be distinguished from dolomite with a simple stain of Alizarin Red-S in a 0.2% HCI solution (cold). Calcite and aragonite turn red, whereas dolomite remains colorless. Dolomite Can be. distinguished from calcite by the above method or one can stain specifically for dolomite with a num-

ber of organic stains including Titan Yellow, Trypan Blue, and Safranine 0 . All these stains require boiling the sample in a concentrated NaOH solution. (Mg) Calcite Can be distinguished from aragonite and lowMg calcite by use of Clayton Yellow stain. This is made by adding 0.5 g of Titan Yellow, 0.8 g of NaOH, and 2 g of EDTA to 500 ml of distilled water. The grain or section is etched in dilute acetic acid for 30 seconds, and is then put in Clayton Yellow solution for 30 minutes. Mg-calcite turns red while low-Mg calcite remains colorless. Mg-calcite can also be stained with Alizarin Red-S in 30% NaOH; calcite remains colorless whereas Mg-calcite turns purple. (Fe) Calcite Can be distinguished (along with ferroan dolomite) from normal calcite by the use of a potassium ferricyanide stain in a weak HCI solution (details in Dickson, 1966). Ferroan minerals turn pale to deep turquoise, and nonferroan ones remain colorless.

•MBF

• • • • •

Upper Permian Tansill Formation New Mexico A n example of Alizarin Red-S staining of a t h i n section. Large echinoderm fragment and other skeletal grains have stained red (calcite) whereas matrix is largely unstained (dolomite). Stains can be preserved w i t h covering of mineral oil or glass cover slip.

0.25 mm

X-Ray Diffraction of Carbonate Rocks ly (in terms of the angle, 2 0) the reflection peak positions representing the (112) plane of the calcite crystal lattice. By matching that data against the chart given below (modified from Goldsmith, Graf, and Heard, 1961) one can approximate the magnesium content of the lattice to about 0.5 mol%. However, other cations besides magnesium can cause lattice spacing shifts and this data should thus be checked occasionally with microprobe or atomic absorption.

In addition to being a fast and reliable method of determing the bulk mineralogy of carbonate rocks (aragonite, calcite, dolomite, siderite, etc.), X-ray diffraction allows the moderately accurate determination of the amount of magnesium (Mg) substitution in the calcite or dolomite lattice. For this, one needs to do careful scans at low chart speeds. By including an internal standard (galena for ancient carbonates and NaCI or CaF2 for modern sediments) one can determine very accurate-

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60

55

50

45

40

35

30

25

MOL PERCENT Mg

20

15

10

5

O

229

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Cathodoluminescence can provide useful information about the spatial distribution of trace elements in carbonates although it does determine which elements are involved. These photos show comparison of the same field of view under plain light microscopy and cathodoluminescence. Note distinction

of two or more generations of cement w i t h complex boundaries in cathodoluminescence photos. Upper samples are f r o m Lower Pennsylvanian Bloyd Formation, Oklahoma; a 1.25 cm scale bar would be 0.25 mm. Lower samples are f r o m Triassic of Austria; a 1.25 cm scale bar would be 0.20 mm.

230

Color photography of cathodoluminescence (although sometimes difficult because of the low light intensities involved) can often yield spectacular results. This example is from the Lower Mississippian Lake Valley Limestone of New Mexico. The upper photograph shows a cement zone in a crinoidal biosparite. From this transmitted light view only one generation of overgrowth cementation would be inferred. The lower photograph illustrates approximately the same field of view, however, and shows that with cathodoluminescence at least five generations of cementation are visible. These cement generations can be correlated from sample to sample and can be related t o a variety of tectonic and erosional events (see Meyers, 1974). A 1.25 cm scale bar would be equal to 0.30 mm on original sample. Photographs courtesy of W. J. Meyers.

231

Scanning electron microscopy (SEM) offers enormous advantages in the 60- to 1 5,00OX-magnification range; easy preparation, excellent resolution, and a much greater depth of focus than with light microscopy. First photo shows details of coccolith morphology and crystal texture in this chalk (Upper Cretaceous Austin Group, 1.3 jum). The great depth of

Transmission electron microscopy allows very high resolution and magnification. Disadvantages include working with polished, etched, and replicated surfaces which may introduce

focus of the SEM allows the observation of whole specimens, such as this Foraminifera Spiriliina decoratali?) shown in the second photo. A 1.25 cm scale bar would be 55 jum. The main difficulties are in correlation of SEM observations w i t h those made w i t h the light microscope.

artifacts, and difficulty of getting low magnification views. Two coccoliths seen here from Upper Cretaceous Monte Antola Formation, Italy. Scale bars are each 2 \im.

232

r^mm.

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Scanning electron microscopy is useful not only for examining sediment textures, but when equipped w i t h an energy dispersive analyzer it can be used effectively for mineral identification and semi-quantitative chemical analysis. The above examples from the Upper Cretaceous Atco Formation (Austin Group) of Texas show accessory minerals in the chalk. The pair of photographs on the left (top and bottom)

illustrate pyrite crystals (about 60 n
Microprobe

The microprobe offers the advantage of getting chemical analyses of areas as small as a few microns or scans of much larger regions. These photographs illustrate one application. The rock was filled with rhombs which were all presumed, on petrographic grounds, to be dolomite. When placed under the microprobe, they were analyzed for calcium (top photos, A, in each of the four series), magnesium (middle photos, 8, in each of the four series), and iron (bottom photos, C). Note that the crystals in the two upper series all contain calcium and magnesium (A and B) while having outer, iron-rich zones (C). The lower t wo series have calcium and iron-rich zones (A and C) but are completely lacking the mag· nesium (B). Thus t he two upper crystals are dolom ite and fer· roan dolomite whereas the bottom two crystals have been dedolomitized (but without losing zonat io n} and are now calcite, and ferroan calcite. Simple petrographic distinction was impossible, although staining or cathodoluminescence might have revealed th e same features. The main disadvantages of the technique are cost, time o f sample preparation, need for accurate standards, and inability t() distinguish many elements in the trace amounts in which they are found in carbonate rocks.