STUDIES ON PALEOZOIC FORAMINIFERA. Chaired by John Groves, Katsumi Ueno and Greg Wahlman

Transcription

1 ISSN Vol / 2006 STUDIES ON PALEOZOIC FORAMINIFERA Chaired by John Groves, Katsumi Ueno and Greg Wahlman Specialists on Paleozoic Foraminifera met in Bellingham (USA) and Ankara (Turkey) in 1997 and 2001, respectively, to discuss advances in the study of foraminiferal evolution, biostratigraphy, paleoecology, paleobiogeography, and systematics. The present Open Session devoted exclusively to Paleozoic Foraminifera is intended to continue the tradition of previous PaleoForams meetings. By combining PaleoForams with Forams2006, however, Paleozoic workers gain the benefit of interaction with specialists on younger fossils and living protists. 213

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3 ISSN Vol / 2006 p Evolutionary trends in the wall composition and structure of Globivalvulina and allied genera in the Carboniferous and Permian Demir Altiner & Sevinç Özkan-Altiner Department of Geological Engineering, Middle East Technical University, Ankara, Turkey demir@metu.edu.tr The wall composition and structure of the genus Globivalvulina and allied genera evolved in 9 distinct trends in the Tournaisian (Carboniferous)- Changxingian (Permian) interval in the Late Paleozoic. Group I, which ranges from Tournaisian to Early Moscovian includes forms with dominantly microgranular wall and a scarcely noticeable hyaline layer (Biserella trend). Group II was derived from the Biseriella trend. It extends from the late Serpukhovian to the end of Permian and includes species of Globivalvulina whose microgranular wall is accompanied by a variably developed inner fibrous layer. Group III derived from Group I and ranges from Late Bashkirian to Moscovian. The wall in Group III, typified by Tenebrosella, is thick and layered microgranular to granular in appearance. Group IV (Bashkirian to Kasimovian), probably derived from Group II, and is characterized by a well-defined inner fibrous layer and an outer thick microgranular to granular wall (G. ex gr. granulosa trend). Simple and microgranular walled groups (V and VI) were derived iteratively from Group II in the Moscovian-Early Permian (G. pulchra- G. vulgaris trend) and Middle-Late Permian (Globivalvulina decrouezae trend) intervals. Groups V and VI, however, could also be interpreted as a continuation of the Biseriella trend. A fundamental and well defined lineage in the Permian is the G. graeca- G. vondershmitti Group (VII), whose wall consists of three layers: an outer translucent, a middle microgranular to granular, and an inconsistenly developed inner fibrous layer. Two distinct wall types were derived from this group in the Capitanian, the four-layered wall thickened at the anterior of septa (Group VIII, Charliella trend) and a double layered wall with outer translucent and inner dense microgranular layers represented by the G. cyprica trend (Group IX). 215

4 Evolutionary trends in the wall composition and structure of Globivalvulina and allied genera in the Carboniferous and Permian Demir Altiner & Sevinç Özkan-Altinert The evolution of biseriamminid foraminifers accelarated considerably in the Capitanian-Changxingian interval. The G.gracea-G.vonderschmitti lineage constitued the root stock of Paraglobivalvulina, while G. decrouezae gave rise to the Septoglobivalvulina-Paraglobivalvulinoides lineage. The dagmaritins, characterized by angular chambers in the adult stage, were derived from G. cyprica and split into several lineages in the Middle to Late Permian. 216 Anuário do Instituto de Geociências - UFRJ ISSN Vol / 2006 p

5 ISSN Vol / 2006 p. 217 Morphology and systematics of biserially enrolled fusulinoidean foraminifera with replaced or recrystallized wall structure Demir Altiner 1 ; John R. Groves 2 ; Sevinç Özkan-Altiner 1 ; I. Ömer Yilmaz 1 & Ayse Atakul 1 1 Department of Geological Engineering, Middle East Technical University, Ankara, Turkey demir@metu.edu.tr 2 Department of Earth Science, University of Northern Iowa, Cedar Falls , U.S.A. Although staffellids originated from pseudoendothyrids in the mid- Carboniferous, the generic diversification of the group occurred in the Permian. Most staffellid genera are characterized by discoidal, lenticular, or spherical shells. Unusual staffellids with oval or fusiform axial profiles appeared in the Middle Permian. Among the elongated Permian staffellids, the subfamily Thailandininae is a highly derived group characterized by numerous volutions, the presence of parachomata, and transverse septula. All staffellids (including thailandinins) are distinct from other fusulinoideans in possessing variably recrystallized or replaced test walls. The altered walls are interpreted to have been originally aragonite or high-mg calcite in composition, in contrast to the microgranular low-mg calcite of other fusulinoideans. The present study describes a novel morphology in staffellids from the Middle Permian (Capitanian) of Turkey. This new forms are characterized by ovate shells with rounded to acute poles and axially elongated, biserially enrolled chambers. Chomata are absent, but features resembling inconsistently developed parachomata are present in the part of the test where biserially enrolled chambers overlap. Circular foramina occur in two rows at the base of the antetheca and septa. Although not well preserved, wall structure is probably keriothecal. The new forms are assigned to the Thailandininae on the basis of their axial elongation, keriothecal wall structure, parachomata, and apertural system. They are unlike any known fusulinoidean in possessing biserially arranged chambers. 217

6 ISSN Vol / 2006 p. 218 Palynoforaminifera in the Silurian-Devonian Amazon Basin, Brazil Tereza Regina Machado Cardoso & Maria Antonieta da Conceição Rodrigues UERJ, Rua São Francisco Xavier, 524/2032A, Faculdade de Geologia, , Rio de Janeiro, Brazil tutucauerj@gmail.com The term palynoforaminifera was created to describe internal organic remains of microforaminiferal tests recovered from the maceration of sedimentary rocks for palynological studies. Different nomenclatural schemes have been developed on the basis of biological criteria and on the size of palynoforaminifera. The first category (biological criteria) utilizes the term Scytinascia to denote the organic remains of benthonic foraminifera. A second, informal scheme is based on the morphology of fossil and recent morphogroups, having as the main factor the arrangement of chambers. The main morphogroups are represented by simple chambers in uniserial, biserial, spiraled, or combined arrangements. Their potential as paleoenvironmental indicators is the main reason for the study of palynoforaminifera. They have been used in paleoenvironmental and paleogeographic reconstructions, for recognition of sedimentary cycles and background stagnation conditions, for marine water temperature estimates linked to ressurgency phenomena, and for climatic cooling due to glaciation. The term microforaminiferal linings has been applied to the organic remains of microforaminifera. Grayson (1956) believed that calcitic tests were not destroyed by the standard hydrofluoric acid treatment for the removal of siliceous matter, and also that no reaction occurred when the remains were subsequently treated with hydrochloric acid. If this assumption is valid, palynoforaminifera should not be present after treatment with hydrochloric acid following hydrofluoric acid. Thus, as Hoffmeister (1955) concluded, the survival of originally calcareous or arenaceous foraminiferal remains is due to the presence of an acid-resistant (chitin or sporepollenin) inner lining. Palynoforaminifera in Permian, Cretaceous and Cenozoic marine sections in Brazilian sedimentary basins are relatively common. A palynological examination of Silurian-Devonian marine samples from the Amazon Basin revealed their presence also. The occurrence of spiraled and complex palynoforaminifera morphotypes associated with acritarchs, chitinozoa and scolecodonts indicates a shallow marine environment during Silurian-Devonian time in the Amazon basin. 218

7 ISSN Vol / 2006 p Paleogeography of Upper Paleozoic carbonates in the Indochina block of Thailand based on fusulinoidean data Titima Charoentitirat Department of Geology, Faculty of Science, Chulalongkorn University Bangkok 10330, Thailand ctitima@geo.sc.chula.ac.th Paleogeographic reconstruction of Upper Paleozoic carbonates along the western margin of the Indochina Block of Thailand is based on lithostratigraphic and biostratigraphic correlations as well as microfacies analysis. The biostratigraphy of Upper Paleozoic fusulinoidean faunas, especially their regional similarities within the Indochina Block of Thailand, is known only on the basis of preliminary work. A summary of recent information on the fusulinoidean biostratigraphic zonation of the Upper Carboniferous through Middle Permian in this area is provided in the present study. Lithologically, Lower to Upper Carboniferous rocks in the Loei- Phetchabun Foldbelt area are represented by nearshore sandstone, shale, thinbedded limestone or limestone lenses and conglomerate, whereas Permian rocks are dominantly thick-bedded limestone, siliciclastics and chert (Mantajit, The International Conference on Stratigraphy and Tectonic Evolution of Southeast Asia and the South Pacific, Bangkok, Thailand, August 1997: 1-26). Wielchowsky & Young (1985. Conference on Geology and Mineral Resources Development of the Northeast Thailand, Khon Kaen University, Khon Kaen, Thailand: 41-55) divided the Permian carbonate rocks in the western rim of the Indochina Block in Thailand into the Pha Nok Khao Platform in the east, the Khao Khwang Platform to the west and the Nam Duk Basin situated between the two platforms. According to fusulinoidean studies (Igo, Geol. Palaeont. Southeast Asia, 10: ; Toriyama, Mem. Fac. Sci., Kyushu University, Series D, Geology, 23 (1): 1-116; Toriyama & Kanmera, Geol. Palaeont. Southeast Asia, 20: 23-93; Ingavat et.al, Geol. Paleont. Southeast Asia, 21: 43-62; Ueno and Igo, Trans. Proc. Palaeont. Soc. Japan, N.S. (171): ; Charoentitirat, Master Thesis, University of Tsukuba, Japan, Doctoral Thesis, University of Tsukuba, Japan.), the carbonate successions of the Pha Nok Khao Platform have high generic diversity in terms of Late Carboniferous and Early Permian fusulinoideans. In contrast, Middle Permian fusulinoideans are 219

8 Paleogeography of Upper Paleozoic carbonates in the Indochina block of Thailand based on fusulinoidean data Titima Charoentitirat less diverse in this platform. In the Khao Khwang Platform, the diversity of Late Carboniferous and Early Permian fusulinoideans is low, whereas Middle Permian diversity is high. Lower Carboniferous and Upper Permian carbonates are subordinate to siliciclastics in these two platforms, suggesting that the sea was quite restricted or that conditions were not suitable for fusulinoideans and carbonate deposition. However, recent biostratigraphic analysis of the Upper Paleozoic carbonate succession distributed along the western part of the Indochina Block of Thailand indicates that the platforms belonged to Tethyan biogeographic province, as Tethyan fusulinoidean taxa predominate in these regions. The Nam Duk Basin between the two platforms contains mainly siliciclastic turbidites, is relatively narrow, and is not a true deep basin. Tectonically, the Nam Duk area is part of a back-arc basin (Chonglakmani, Gondwana Research, 4 (4): ). The source of the sediments in the Nam Duk Basis is still questionable. Based on fusulinoideans found in limestone bodies and lithostratigraphic studies in the Nam Duk Basin (Chutakositkanon et al., Charoentiti Proceedings of the International Conference on Stratigraphy and Tectonic Evolution of Southeast Asia and the South Pacific, Bangkok, Thailand: 368), some siliciclastic sediments and limestones in the basin were derived from foreland areas or the two platforms located to the east and west of the basin. 220 Anuário do Instituto de Geociências - UFRJ ISSN Vol / 2006 p

9 ISSN Vol / 2006 p Permian foraminifera from northeast Gondwana David W. Haig The University of Western Australia,Australia - dhaig@segs.uwa.edu.au The western margin of the present Australian continent, extending from the islands of the Outer Banda Arc in the north, down the Australian North West Shelf to southwest Australia, contains a sedimentary record of Permian basins that lay in the interior of northeast Gondwana. The Permian continental shelf is not preserved along this margin, having been rifted prior to the Late Jurassic. The preserved Permian deposition took place in narrow elongate interior-rift basins where siliciclastic sand-shale deposition dominated. Carbonate platforms, built of mainly heterozoan grain assemblages (brachiopod-bryozoancrinoid debris), developed in some of the basins for short intervals, and volcaniclastic units are also known in some areas. The stratigraphic architecture of the undeformed basins includes laterally continuous strata that remain horizontal and suggest shallow-water depositional conditions. This presentation will review foraminifera known from the Perth, Carnarvon and Canning Basins of Western Australia, and from the Gondwanan Sequence in Timor Leste. The assemblages are of two types: mud-facies microfaunas and carbonate-platform microfaunas. Organic-cemented agglutinated foraminifera usually dominate the mud-facies assemblages and are preserved as deformed siliceous tests rigidly cemented by quartz overgrowths. Genera include Aaptotoichus, Ammobaculites, Ammodiscus, Ammovertella, Glomospirella, Haplophragmoides, Hyperammina, Kechenotiske, Lagenammina, Palustrella, Placentammina, Psammosphaera, Reophax, Sansabaina, Spiroplectammina, Thuramminoides, Trochammina, and Trochamminopsis. At various levels calcareous hyaline foraminifera are present (including Howchinella, Lunucammina, Nodosaria, Protonodosaria, and Vervilleina). The carbonate-platform assemblages include Calcitornella- Trepeilopsis dominated assemblages in the Sakmarian of the Carnarvon and Perth Basins, Abadehella-dominated assemblages of the mid-permian of the Perth Basin, and low diversity fusuline assemblages at various levels in the Gondwanan sequence of Timor. The lithostratigraphic and biostratigraphic successions reflect the variable marine conditions that existed during the Permian in the interior basins. The 221

10 Permian foraminifera from northeast Gondwana David W. Haig faunal associations in the basins record salinity and temperature changes associated with the melting of the Gondwanan Continental Ice Sheet during the Asselian-Sakmarian, and later high-frequency cycles of bathymetric change (of combined tectonic and eustatic origin). The biogeographic relationships of the Australian Permian fauna should be viewed in the light of an interior-basin setting. At present, it is not possible to compare the microfauna with that of the Permian open continental shelf of northeast Gondwana, as this has rifted from the Australian continent and now may be incorporated in various deformed terranes in southeast Asia. 222 Anuário do Instituto de Geociências - UFRJ ISSN Vol / 2006 p

11 ISSN Vol / 2006 p Moscovian-Kasimovian and Kasimovian-Gzhelian boundaries in the Donets Basin, Ukraine: Current perspective from fusulines Katsumi Ueno Department of Earth System Science, Faculty of Science, Fukuoka University, Fukuoka Japan katsumi@fukuoka-u.ac.jp The Kalinovo section (Aizenberg et al., Field Excursion Guidebook for the Donets Basin. Publishing Office Nauka, Moscow, 360 p.) in the eastern part of the Donets Basin, Ukraine, exhibits a continuous, late Moscovian-Gzhelian paralic succession with cyclic, fossiliferous (particularly fusulines and conodonts) carbonate intercalations. This section allows examination of fusuline faunas spanning two late Pennsylvanian stage boundaries: the Moscovian-Kasimovian boundary and the Kasimovian-Gzhelian boundary. Despite its biostratigraphic importance within the Donets Basin, the details of the fusuline faunal succession have not been properly investigated until now. The Kalinovo section is certain to provide key information for the eventual formal definition and GSSP selection associated with these two boundaries. The Kalinovo No. 1 section covers the upper part of the C 3 1 (N) and the lower part of the C 3 2 (O) Suites, ranging from limestone N 2 to O 4, in which N 2, N 3, N 31, N 32, N 33, N 51, O 1, O 11, O 12, O 2, O 3, and O 4 crop out. In N 2, typical late Moscovian genera such as Taitzehoella and Fusulina are found. N 3 yields Quasifusulinoides and primitive Protriticites, thus suggesting a latest Moscovian (late Myachkovian) age. N 3 3 records the occurrence of Protriticites similar to P. pseudomontiparus and/or P. subschwagerinoides, and is probably already of traditional, early Kasimovian (Krevyakinian) age. O 1 is dominated by Obsoletes and Quasifusulinoides. This level is possibly correlated to the later part of the traditional early Kasimovian (late Krevyakinian) or the early part of the traditional middle Kasimovian (early Khamovnikian). O 2 is rich in typical Montiparus, and is probably correlated to the later part of the traditional middle Kasimovian (late Khamovnikian). In O 3, Quasifusulina is dominant, which suggests a traditional late Kasimovian (Dorogomilovian or younger) age. In the Kalinovo No. 1 section, therefore, the traditional base of the Kasimovian can be placed somewhere within the N 3 -N 3 3 interval. In the Donets Basin, O 1 223

12 Moscovian-Kasimovian and Kasimovian-Gzhelian boundaries in the Donets Basin, Ukraine: Current perspective from fusulines Katsumi Ueno exhibits the first appearance datum of Idiognathodus sagittalis, which is regarded provisionally as a potential maker conodont for the base of the Kasimovian (Villa & Task Group, Newsletter on Carboniferous Stratigraphy, 23: 9-10.). Thus, this level is several depositional cycles higher than the traditional base of the Kasimovian if each limestone in the Donets Basin corresponds to a single transgressive-regressive sea-level cycle (Heckel et al., Newsletter on Carboniferous Stratigraphy, 23: ). The Kalinovo No. 2 section, located SW of the Kalinovo No. 1 section, encompasses the upper part of the C 3 2 (O) Suite, spanning from limestone O 4 1 to O 7. Of the limestones, O 41, O 42, O 43, O 5, O 6, O 61, and O 7 were collected for this study. The first three limestones are barren of fusulines. O 5 yields Triticites similar to T. irregularis and Rauserites rossicus, the latter of which is a conventional marker for the basal part of the Gzhelian (C 3 C 1 ) in the Moscow Basin and several other areas of Eurasia (Rauser-Chernousova et al., Geological Society, Occasional Publication, 4: ). O 7 also contains R. rossicus that is probably slightly more advanced than the population from O 5. Idiognathodus simulator is regarded as a potential marker conodont for the Kasimovian-Gzhelian boundary, and it first occurs in O 7 in the Donets Basin (Villa & Task Group, 2005). Thus, the taxonomic justification of two Rauserites rossicus from O 5 and O 7 is the next important challenge to cope with for better understanding the Kasimovian-Gzhelian boundary in the Donets Basin. 224 Anuário do Instituto de Geociências - UFRJ ISSN Vol / 2006 p

13 ISSN Vol / 2006 p Radiation of the fusulinoideans between the two phases of the end-permian mass extinction, South China Wang Yue & Jin Yugan State Key Laboratory of Palaeobiology and Stratigraphy, Nanjing Institute of Geology and Palaeontology, CAS, China yuewang@nigpas.ac.cn The end-permian mass extinction is the largest bioevent in geological history. Benthic groups such as fusulinids, corals and bryozoans, nevertheless, suffered most severely at the end of Guadalupian, which is regarded as the first phase of the event. As a consequence of the pre-lopingian global regression, the large-scale carbonate platforms that were habitats for the endemic benthic fauna disappeared in peri-pangean, as well as in the relic shelves in Paleotethys. Changes to the ecosystem were disastrous for the benthos living in carbonate environments. Among them, the fusulinoideans suffered a generic extinction rate of 76% globally, and 87% in South China. Those capable of living in environments other than carbonate platforms survived and became the dominant figures of the Wuchiapingian. For example, the genera Codonofusiella and Reichelina were so abundant in Wuchiapingian that they formed the Codonofusiella fossil zone in South China. The diversification of new genera in the Late Permian didn t start until the Changhsingian Stage, when Palaeofusulina minima appeared as a pioneer in the lower Changhsingian and P. sinensis appeared as advanced form in the upper Changhsingian. Thus the genus Palaeofusulina was regarded as the index fossil for the Changhsingian Stage. However, recent studies on the Capitanian-Wuchiapingian boundary led to the discovery of the Wuchiapingian Palaeofusulina fauna in Penglaitan, Laibin county, Guangxi Province. The fauna is composed mainly of large-sized and long-fusiform forms as well as a few small fusiform morphologies. New data on the genus made it necessary to re-evaluate its evolution pattern because there exists an evolutionary vacuum between the supposed ancestor Dunbarula and Changhsingian Palaeofusulina. In this cladistic analysis, 10 species were selected, including the 6 subgroups of Palaeofusulina, the type species of Nanlingella and Parananlingella, and the newly discovered species of Palaeofusulina and Gallowayinella in Penglaitan, with Dunbarula mathieui 225

14 Radiation of the fusulinoideans between the two phases of the end-permian mass extinction, South China Wang Yue & Jin Yugan as outgroup. The result shows that the two morphologic types of Palaeofusulina in the early Wuchiapingian represent two evolutionary lineages. One clade includes long-fusiform types such as Gallowayinella sp. A and Palaeofusulina sp. A, which originated in the early Wuchiapingian and became less abundant during the Changhsingian. The other is represented by the small and fusiform species, the dominant group of P. minima P. sinensis P. ellipsoidalis P. prisca in the Changhsingian. Among the fusulinoidean genera that appeared in the Upper Permian, nearly 70% developed in a short period of time soon after the Pre-Lopingian crisis. An analysis of Late Permian fusulinid evolutionary change and paleogeography suggests that rebound and final extinct of fusulinids during their survival phase coincide closely with the appearance and elimination of small-scaled isolated carbonate platform in Southwest China. 226 Anuário do Instituto de Geociências - UFRJ ISSN Vol / 2006 p