The report revises and expands upon the 1976 and 1978 publications for the Dinantian and Silesian, respectively, combining them into a single account of British and Irish Carboniferous stratigraphy. The need to update the two Special Reports reflects the considerable advances in Carboniferous geology over the last 30 years. The report covers developments in international chronostratigraphy and incorporates wholesale reassessments of British lithostratigraphy. A huge volume of biostratigraphical information has been published over recent decades and the report summarizes the key information.Carboniferous rocks have long been of economic importance, but it is the search for hydrocarbons, in its infancy at the time of the previous reports, which has greatly increased our understanding of Carboniferous successions offshore and at depth, particularly in southern and eastern England.

Four graptolite biozones are recorded from the Arenig portion of the Road River Group in the Richardson and Mackenzie mountains in the Yukon and Northwest Territories. In ascending order, these zones are Tetragraptus approximatus, Pendeograptus fruticosus, Didymograptus bifidus, and Parisograptus caduceus australis (new). The Castlemainian stage may be represented by nongraptolitic massive bedded chert. The Arenig–Llanvirn boundary is drawn below the first occurrence of Undulograptus austrodentatus. Fifty-four graptolite taxa are present, and 16 of these species and subspecies are recorded for the first time in this deep-water biotope, namely, Didymograptus? cf. adamantinus, D. asperus, D. dilatans, D. cf. kurcki, D. validus communis, Holmograptus aff. leptograptoides, H. sp. A, Isograptus? sp. nov. A, I. ? dilemma, Keblograptus geminus, Pseudisograptus manubriatus harrisi, Ps. m. koi, Ps. m. janus, Ps. cf. tau, Xiphograptus lofuensis, and Zygograptus cf. abnormis.

Over the years a number of individuals have inquired about pollen/nectar plants in central Minnesota. When Minnesota's Department of Ag also asked, I began a year of photography to prepare this article. Many people are not really aware of what their bees are working, nor are they always able to identify floral sources. With more than forty years to get a. "handle" on this information, this gives me a chance to share with a wider audience. It was also among the most enjoyable articles I've put together for you. Who doesn't get a charge out of looking at plant life in its glory, especially if he's a beekeeper?

Graptolite zones of early and late Tremadoc ages are described from the Elmer Creek Formation in the Selwyn Basin and from the Duo Lake Formation in the Misty Creek Embayment. In ascending order, these are: Staurograptus dichotomus, Anisograptus matanensis, Adelograptus cf. A. tenellus and Aorograptus victoriae Biozones. The uppermost zone embraces the Adelograptus antiquus Biozone, Kiaerograptus? pritchardi Biozone, and the Paradelograptus kinnegraptoides Biozone in the Richardson Trough. Twenty five species are recorded and fourteen species are described, including the first record of the Rhabdinopora fauna in the early Tremadoc of northwest Canada and Kiaerograptus magnus Williams and Stevens and Paratemnograptus isolatus Williams and Stevens in the late Tremadoc. When modifications to Cooper's (1999) ecostratigraphic model are made based on data from Yukon and Northwest Territories, the upper slope biotope and lower slope - ocean-floor biotope become so similar that there is little basis for recognising both biotopes.

Twenty-two graptolite species are described from the Tremadoc portion of the Road River Group. In a 220 m thick, graptolite-rich section on Peel River, six graptolite biozones are recognized which in ascending order are: Staurograptus dichotomus, Anisograptus matanensis, Adelograptus cf. A. tenellus, Adelograptus antiquus, Kiaerograptus pritchardi and Paradelograptus kinnegraptoides. The Psigraptus fauna appears to be confined to a single bedding-plane within a thick interval dominated by Adelograptus cf. A. tenellus, and for this reason we propose a new zone characterized by the latter species rather than identify a Psigraptus Biozone as in China. The Adelograptus cf. A. tenellus Biozone has yielded Adelograptus? bulmani Spjeldnaes 1963, which we propose as the type species for the new genus Ancoragraptus. Graptolites recorded from the Tremadoc of the Yukon for the first time are: Ancoragraptus bulmani, Clonograptus magnificus, C. cf. C. multiplex, C. cf. C. rigidus, Hunnegraptus copiosus, Kiaerograptus? bulmani and K? kutchini sp. nov.

The Glenogle Formation (age: Arenig to very early Caradoc) accumulated in the White River Trough between the Purcell Platform to the west and the Bow Platform to the east. The formation is up to 851 m thick, its basal contact is conformable with the McKay Group, and the upper contact is an unconformity below Upper Ordovician rocks that elsewhere cuts down as low as into the Precambrian. The Upper Member of the Glenogle has significant contents of quartz silt and sand within successions of shale in western outcrops and within dolomite in eastern outcrops. The Lower Member is dominantly shale and limy shale but, in eastern outcrops, can be divided into four units (basal, cherty quartz siltstone, middle, and limestone units) by means of incursions of detrital carbonate and siliceous sediments that were swept into the White River Trough from the Bow Platform. Debris flows within western outcrops of the Lower Member demonstrate the presence of shallow-water carbonate rocks on the Purcell Platform during early Llanvirn time. Thermal maturities are high in the Glenogle Formation (Conodont Alteration Indices mostly 4-5; Graptolite Maximum Reflectances 7.93-11.9%). Graptolites are prominent in the Glenogle Formation and the Pendeograptus fruticosus-Tetragraptus approximatus, Didymograptus bifidus, Isograptus victoriae maximus, Oncograptus, Cardiograptus, Paraglossograptus tentaculatus, Pseudoclimacograptus decoratus, "Glyptograptus" euglyphus and Nemagraptus gracilis zones are recognized and can be correlated with precision with graptolite sequences in Australia, New Zealand, Newfoundland, and Spitsbergen. The local presence of shelly fossils and recovery of conodonts from a few stratigraphic sections allow correlations between the graptolitic facies of the Glenogle Formation and the Spitsbergen sequence and with the platform facies of the North American craton. The upper part of the Ibexian Series is correlated with the Bendigonian, Chewtonian and lower Castlemanian stages; the Orthidiella and Anomalorthis zones of the lower Whiterockian Series with the upper Castlemanian, Yapeenian and the Darriwilian stages; and the Valhallan Stage of Spitsbergen with the late Bendiognian to early Darriwilian. The Prioniodus elegans Conodont Zone of the Atlantic Faunal Realm and the Oepikodus communis and Jumudontus gananda-Reutterodus andinus zones of the Midcontinental Faunal Realm are at least partly correlative with the D. bifidus Zone. Conodonts of early Whiterockian age occur with graptolites of the I. v. maximus Zone. Conodonts representing the Histiodella altifrons Zone occur in the Cardiograptus Zone and also just above the graptolites of the Oncograptus Zone. Faunas representative of the interval Lenodus variabilis Zone to Eoplacognathus suecicus Zone are present within the P. decoratus Zone and also directly above the P. tentaculatus Zone. Faunas with Phragmodus flexuosus occur above the P. decoratus Zone and below the "G." euglyphus Zone. The Pygodus serra Zone is represented within the upper part of the "G." euglyphus Zone.

Ten graptolite species from upper Tremadoc and lower Arenig strata are described from a 160 m thick, homoclinal, totally exposed section of the Road River Group in the Upper Canyon of Peel River, Yukon. This is believed to be one of the most complete sequences of this age range known to science. Graptolites were collected from 40 levels in the (lowest to highest) Adelograptus antiquus, Kiaerograptus pritchardi, Paradelograptus kinnegraptoides, Tetragraptus approximatus, and Pendeograptus fruticosus biozones. Two new species described are Paradelograptus rallus sp.nov. from the K. pritchardi Biozone and Kinnegraptus reclinatus sp.nov. from the Tetragraptus fruticosus Biozone.

Abstract The Lower Permian and Triassic successions of the offshore East Irish Sea Basin are probably the thickest of the United Kingdom Continental Shelf or UK mainland, but currently, no hierarchical lithostratigraphy exists for this offshore area. A summary is presented of the first comprehensive hierarchical lithostratigraphical nomenclature scheme to be established for the Carboniferous, Permian and Triassic rock successions of the offshore East Irish Sea Basin. This scheme, which has been sponsored by interested exploration companies, identifies 25 formal lithostratigraphical divisions following the methodology already established in BGS-UKOOA (British Geological Survey-United Kingdom Offshore Operators’ Association) revisions of North Sea lithostratigraphy. Sixteen new lithostratigraphical names are introduced (nine in the Mercia Mudstone Group, one in the Sherwood Sandstone Group, three each within the Permian and Carboniferous successions). The lithology, wireline log characteristics and nature of the lower boundary are discussed briefly for each lithostratigraphical unit, together with correlations to the adjacent onshore successions where appropriate. Formal definitions of lithostratigraphic units, including type and reference sections are fully documented elsewhere. The aims of this study are to rationalize the existing terminology and to provide a practical scheme that will have the widest acceptance within the oil industry.

Research Article| November 01, 1969 Siluro-Devonian Boundary in North America1 J. M BERDAN; J. M BERDAN U.S. Geological Surrey, E-501 U.S. National Museum, Washington, D.C. Search for other works by this author on: GSW Google Scholar W. B. N BERRY; W. B. N BERRY Department of Paleontology, University of California, Berkeley, California Search for other works by this author on: GSW Google Scholar A. J BOUCOT; A. J BOUCOT Department of Geology, University of Pennsylvania, Philadelphia, Pennsylvania PRESENT ADDRESS: OREGON STATE UNIVERSITY, CORVALLIS, OREGON (BOUCOT AND JOHNSON) Search for other works by this author on: GSW Google Scholar G. A COOPER; G. A COOPER U.S. National Museum, Washington, D.C. Search for other works by this author on: GSW Google Scholar D. E JACKSON; D. E JACKSON Department of Geology, University of Alberta, Edmonton, Alberta Search for other works by this author on: GSW Google Scholar J. G JOHNSON; J. G JOHNSON Department of Geology, University of Pennsylvania, Philadelphia, Pennsylvania PRESENT ADDRESS: OREGON STATE UNIVERSITY, CORVALLIS, OREGON (BOUCOT AND JOHNSON) Search for other works by this author on: GSW Google Scholar GILBERT KLAPPER; GILBERT KLAPPER Department of Geology, University of Iowa, Iowa City, Iowa Search for other works by this author on: GSW Google Scholar A. C LENZ; A. C LENZ Department of Geology, University of Western Ontario, London, Ontario Search for other works by this author on: GSW Google Scholar ANDERS MARTINSSON; ANDERS MARTINSSON Institute of Palaeontology, Fack, Uppsala 1, Sweden Search for other works by this author on: GSW Google Scholar W. A OLIVER, JR.; W. A OLIVER, JR. U.S. Geological Survey, E-501 U.S. National Museum, Washington, D.C. Search for other works by this author on: GSW Google Scholar L. V RICKARD; L. V RICKARD New York State Museum and Science Service, Albany, New York Search for other works by this author on: GSW Google Scholar R THORSTEINSSON R THORSTEINSSON Institute of Sedimentary and Petroleum Geology, 3303-33rd Street, N.W., Calgary, Alberta Search for other works by this author on: GSW Google Scholar GSA Bulletin (1969) 80 (11): 2165–2174. https://doi.org/10.1130/0016-7606(1969)80[2165:SBINA]2.0.CO;2 Article history received: 03 Feb 1969 first online: 02 Mar 2017 Cite View This Citation Add to Citation Manager Share Icon Share Twitter LinkedIn Tools Icon Tools Get Permissions Search Site Citation J. M BERDAN, W. B. N BERRY, A. J BOUCOT, G. A COOPER, D. E JACKSON, J. G JOHNSON, GILBERT KLAPPER, A. C LENZ, ANDERS MARTINSSON, W. A OLIVER, L. V RICKARD, R THORSTEINSSON; Siluro-Devonian Boundary in North America. GSA Bulletin 1969;; 80 (11): 2165–2174. doi: https://doi.org/10.1130/0016-7606(1969)80[2165:SBINA]2.0.CO;2 Download citation file: Ris (Zotero) Refmanager EasyBib Bookends Mendeley Papers EndNote RefWorks BibTex toolbar search Search Dropdown Menu toolbar search search input Search input auto suggest filter your search All ContentBy SocietyGSA Bulletin Search Advanced Search Abstract The writers note a convergence of opinion on a world-wide scale favoring placement of the Siluro-Devonian boundary at the base of the Gedinnian. This boundary is coincident with the base of the Monograptus uniformis and Icriodus woschmidti zones. It is recognizable in the brachiopod-coraltrilobite succession by the disappearance of pentamerids, Atrypella, Gracianella, halysitids, and Encrinurus and by the incoming of terebratulids, Cyrtina, and common Schizophoria. Insofar as the Pridoli-Lochkov boundary in Bohemia can be revised to correspond to this boundary, the Pridoli is recognized as the uppermost Silurian Stage.In North America, the base of the Devonian, defined as the base of the Gedinnian, is located at what is probably the most satisfactory level because it lies at or near the base of the Helderbergian, which has traditionally been regarded as the lower-most Lower Devonian stage in eastern North America.Seven regions in North America are chosen for discussion because they are representative and form standards of a sort, with which most other fossiliferous sections in North America can be compared. Only in one region does the Siluro-Devonian boundary appear to coincide with a formation boundary, namely, at the base of the St. Alban Formation of eastern Gaspé. It falls within the Stonehouse Formation of Arisaig, Nova Scotia; the Rondout Formation of New York and New Jersey; the Keyser Limestone of western Maryland and vicinity; the Roberts Mountains Formation of central Nevada; the Prongs Creek Formation of Yukon Territory; and the Devon Island and Cape Phillips Formations in the Canadian Arctic Islands. This content is PDF only. Please click on the PDF icon to access. First Page Preview Close Modal You do not have access to this content, please speak to your institutional administrator if you feel you should have access.