DOI: 10.1346/ccmn.1969.0170605. Polytypism of Trioctahedral 1:1 Layer Silicates

Polytypism of Trioctahedral 1:1 Layer Silicates

10.1346/ccmn.1969.0170605

Crossref journal-article

Cambridge University Press (CUP)

Clays and Clay Minerals (56)

Abstract

AbstractPolytypism in trioctahedral 1 : 1 phyllosilicates results from two variable features in the structure. (1) The octabedral cations may occupy the same set of three positions throughout or may alternate regularly between two different sets of positions in successive layers. (2) Hydrogen bonding between adjacent oxygen and hydroxyl surfaces of successive layers can be obtained by three different relative positions of layers: (a) direct superposition of layers, (b) shift of the second layer by a/3 along any of the three hexagonal X-axes of the initial layer, with a positive or negative sense of shift determined uniquely by the octahedral cation set occupied in the lower layer, and (c) shift of the second layer by ± b/3 along Y1 (normal to X1) of the initial layer regardless of octahedral cation sets occupied. Assuming ideal hexagonal geometry, no cation ordering, and no intermixing in the same crystal of the three possible types of layer superpositions, then twelve standard polytypes (plus four enantiomorphs) with periodicities between one and six layers may be derived. Relative shifts along the three X-axes lead to the same layer sequences derived for the micas, namely 1M, 2M1, 3T, 2M2, 2Or, and 6H. Polytypes 1T and 2H1 result from direct superposition of layers. Layer shifts of b/3 lead to polytypes designated 2T, 3R, 2H2, and 6R. The twelve standard 1 : 1 structures can be divided into four groups (A = 1M, 2M1, 3T; B = 2M2, 2Or, 6H; C = 1T, 2T, 3R; D = 2H1, 2H2, 6R) for identification purposes. The strong X-ray reflections serve to identify each group and the weaker reflections differentiate the three structures within each group. Examples of all four groups and of 9 of the 12 individual structures have been identified in natural specimens. Consideration of the relative amounts of attraction and repulsion between the ions in the structures leads to the predicted stability sequence group C > group D > group A > group B, in moderately good agreement with observed abundances of these structural groups.

Bibliography

Bailey, S. W. (1969). Polytypism of Trioctahedral 1:1 Layer Silicates. Clays and Clay Minerals, 17(6), 355â371.

Authors 1

S. W. Bailey (first)

References 27 Referenced 93

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{'key': 'S0009860400027063_bib11', 'first-page': '394', 'article-title': 'The structure of dickite: Z', 'volume': '83', 'author': 'Gruner', 'year': '1932', 'journal-title': 'Krist.'} / Krist. / The structure of dickite: Z by Gruner (1932)
{'key': 'S0009860400027063_bib15', 'first-page': '683', 'article-title': 'A refinement of the dickite structure and some remarks on polymorphism in kaolin minerals', 'volume': '32', 'author': 'Newnham', 'year': '1961', 'journal-title': 'Mineral. Mag.'} / Mineral. Mag. / A refinement of the dickite structure and some remarks on polymorphism in kaolin minerals by Newnham (1961)
{'key': 'S0009860400027063_bib13', 'first-page': '529', 'article-title': 'Random structures of layer minerals as illustrated by cronstedtite (2FeO Fe2-O3-SiO2-2H2O). Possible iron content of kaolin', 'volume': '24', 'author': 'Hendricks', 'year': '1939b', 'journal-title': 'Am. Mineralogist'} / Am. Mineralogist / Random structures of layer minerals as illustrated by cronstedtite (2FeO Fe2-O3-SiO2-2H2O). Possible iron content of kaolin by Hendricks (1939b)
{'key': 'S0009860400027063_bib4', 'first-page': '819', 'article-title': 'Chlorite polytypism—1. Regular and semi-random one-layer structures', 'volume': '47', 'author': 'Bailey', 'year': '1962', 'journal-title': 'Am. Mineralogist'} / Am. Mineralogist / Chlorite polytypism—1. Regular and semi-random one-layer structures by Bailey (1962)
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{'key': 'S0009860400027063_bib14', 'first-page': '14', 'article-title': 'The crystal structure of a hexagonal Al-serpentine', 'volume': '53', 'author': 'Jahanbagloo', 'year': '1968', 'journal-title': 'Am. Mineralogist'} / Am. Mineralogist / The crystal structure of a hexagonal Al-serpentine by Jahanbagloo (1968)
{'key': 'S0009860400027063_bib10', 'first-page': '781', 'article-title': 'Polytypism in cronstedtite', 'volume': '47', 'author': 'Frondel', 'year': '1962', 'journal-title': 'Am. Mineralogist'} / Am. Mineralogist / Polytypism in cronstedtite by Frondel (1962)
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{'key': 'S0009860400027063_bib6', 'first-page': '502', 'article-title': 'The crystal structure of some chamosite minerals', 'volume': '29', 'author': 'Brindley', 'year': '1951', 'journal-title': 'Mineral. Mag.'} / Mineral. Mag. / The crystal structure of some chamosite minerals by Brindley (1951)
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Dates

Type	When
Created	19 years ago (Aug. 28, 2006, 12:27 a.m.)
Deposited	1 month, 2 weeks ago (July 23, 2025, 3:28 a.m.)
Indexed	1 month ago (Aug. 2, 2025, 12:52 p.m.)
Issued	55 years, 9 months ago (Dec. 1, 1969)
Published	55 years, 9 months ago (Dec. 1, 1969)
Published Online	1 year, 2 months ago (July 1, 2024)
Published Print	55 years, 9 months ago (Dec. 1, 1969)

Funders 0

None

BibTeX

@article{Bailey_1969, title={Polytypism of Trioctahedral 1:1 Layer Silicates}, volume={17}, ISSN={1552-8367}, url={http://dx.doi.org/10.1346/ccmn.1969.0170605}, DOI={10.1346/ccmn.1969.0170605}, number={6}, journal={Clays and Clay Minerals}, publisher={Cambridge University Press (CUP)}, author={Bailey, S. W.}, year={1969}, month=dec, pages={355–371} }

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  "abstract": "<jats:title>Abstract</jats:title><jats:p>Polytypism in trioctahedral 1 : 1 phyllosilicates results from two variable features in the structure. (1) The octabedral cations may occupy the same set of three positions throughout or may alternate regularly between two different sets of positions in successive layers. (2) Hydrogen bonding between adjacent oxygen and hydroxyl surfaces of successive layers can be obtained by three different relative positions of layers: (a) direct superposition of layers, (b) shift of the second layer by <jats:italic>a</jats:italic>/3 along any of the three hexagonal X-axes of the initial layer, with a positive or negative sense of shift determined uniquely by the octahedral cation set occupied in the lower layer, and (c) shift of the second layer by \u00b1 <jats:italic>b</jats:italic>/3 along Y<jats:sub>1</jats:sub> (normal to X<jats:sub>1</jats:sub>) of the initial layer regardless of octahedral cation sets occupied. Assuming ideal hexagonal geometry, no cation ordering, and no intermixing in the same crystal of the three possible types of layer superpositions, then twelve standard polytypes (plus four enantiomorphs) with periodicities between one and six layers may be derived. Relative shifts along the three X-axes lead to the same layer sequences derived for the micas, namely 1<jats:italic>M</jats:italic>, 2<jats:italic>M</jats:italic><jats:sub>1</jats:sub>, 3<jats:italic>T</jats:italic>, 2<jats:italic>M</jats:italic><jats:sub>2</jats:sub>, 2<jats:italic>Or</jats:italic>, and 6<jats:italic>H</jats:italic>. Polytypes 1<jats:italic>T</jats:italic> and 2<jats:italic>H</jats:italic><jats:sub>1</jats:sub> result from direct superposition of layers. Layer shifts of <jats:italic>b</jats:italic>/3 lead to polytypes designated 2<jats:italic>T</jats:italic>, 3<jats:italic>R</jats:italic>, 2<jats:italic>H</jats:italic><jats:sub>2</jats:sub>, and 6<jats:italic>R</jats:italic>. The twelve standard 1 : 1 structures can be divided into four groups (<jats:italic>A</jats:italic> = 1<jats:italic>M</jats:italic>, 2<jats:italic>M</jats:italic><jats:sub>1</jats:sub>, 3<jats:italic>T</jats:italic>; <jats:italic>B</jats:italic> = 2<jats:italic>M</jats:italic><jats:sub>2</jats:sub>, 2<jats:italic>Or</jats:italic>, 6<jats:italic>H</jats:italic>; <jats:italic>C</jats:italic> = 1<jats:italic>T</jats:italic>, 2<jats:italic>T</jats:italic>, 3<jats:italic>R</jats:italic>; <jats:italic>D</jats:italic> = 2<jats:italic>H</jats:italic><jats:sub>1</jats:sub>, 2<jats:italic>H</jats:italic><jats:sub>2</jats:sub>, 6<jats:italic>R</jats:italic>) for identification purposes. The strong X-ray reflections serve to identify each group and the weaker reflections differentiate the three structures within each group. Examples of all four groups and of 9 of the 12 individual structures have been identified in natural specimens. Consideration of the relative amounts of attraction and repulsion between the ions in the structures leads to the predicted stability sequence group <jats:italic>C</jats:italic> &gt; group <jats:italic>D</jats:italic> &gt; group <jats:italic>A</jats:italic> &gt; group <jats:italic>B</jats:italic>, in moderately good agreement with observed abundances of these structural groups.</jats:p>",
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