11th Symposium on Fossil Cnidaria and Porifera, Liège, August 19-29, 2011: Abstracts (original) (raw)

2011, Kölner Forum für Geologie und Paläontologie

Abstract

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The classification of habitats of colonial rugose corals during the Mississippian (Carboniferous) of Western Europe is explored, highlighting the evolution of classification systems from broad categories developed by early researchers to a more refined approach integrating various data types. The paper emphasizes the necessity for a classification that accommodates field observations and carbonate facies analyses while addressing challenges in comparing different coral communities across time and space.

Figures (75)

Institut fiir Geologie und Mineralogie der Universitat zu K6In

International Association for the Study of Fossil Cnidaria and Sponges Institut fiir Geologie und Mineralogie, Universitat zu K6In

Fig. 1: Overview on the main characteristics of the types and subtypes. Coral diversity: low (1-3 taxa), moderate (4-7 taxa), high (>7 taxa); Colony distances: close (touching or centimetre scale), moderate (decimetre scale), wide (metre scale); Diversity of other fauna: low (none or few other fauna), moderate (low diverse faunas), high (diverse faunas); Abundance: rare (0-~20% of all exposures), moderate (~20%-~40% of all exposures), common (>~40% of all exposures) (modified from ARETZ 2010). EE iets Leia ae, aaa M. ARETZ, S. DELCULEE, J. DENAYER & E. Poty (Eds.) Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liége, August 19-29, 201:

Fig. 1: Cluster Analysis (Raup-Crick Coefficent; node supports at 1000 bootstrap replicates) for the Westerr European coral province of SANDO (1990). Seven spatial units of late Viséan coral faunas have been differentiated ir Western Europe and Northern Africa. M. ARETZ, S. DELCULEE, J. DENAYER & E. POTY (Eds.) Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liége, August 19-29, 2011

Cyrtophillid corals share a number of characters with three subclasses of An 1) these corals are typically found in remote areas and thus sample sizes are often limited have short geologic ranges and therefore have limited geographic distributions, and specific depositional environments and are not found in upper Ordovician carbonates. T hozoa: Tabulata, Heliolitoidea, and Rugosa. As a consequence, their systematic position within the Anthozoa and even systematics among cyrtophillids remains controversial. The reasons why these controversies persist are that , 2) they typically 3) they occur in herefore, research on cyrtophillids corals has been limited and typically they have not been the focus of individual studies. nstead they are often studied as a component of much larger multidisciplinary studies. Based on new specimens from Mongolia, we are proposing the following new systematic scheme for cyr ophillid corals. Cyrtophyllids are colonial coral that inhabited warm, shallow seas during the Middle-Late Ordovician. LINDSTROM (1882) first described these corals from Siberia. Since then, they have been discovered in the Urals, Taimyr, Gorny Altai, and Northeastern regions of Russia, Arctic islands of Canada, New Jersey state (USA), and Greenland. Mongolian cyrtophillid corals have been found in Ordovician sections of the Khovd, Govi-Altai, and Mandal-Ovoo Terrains in the Central Asian Orogenic Belt (Fig. 1).

Fig. 1: Palaeocene to Miocene coral distribution related to formations and time slices in Oman.

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Fig. 1: (A-C) Results of preliminary phylogenetic analyses focused on clades XIX, XX, and XXI of FUKAMI et al., (2008). A) Single MPT from mitochondrial dataset. B) Strict consensus of 3 MPTs from morphological dataset. C) Strict consensus of 8 MPTs from the combined data analysis. (D-E) Boxplots of the level of phylogenetic signal present in different partitions of the morphological dataset, assessed using the topology and branch lengths from the mitochondrial tree. D) Lambda (PAGEL 1999), with tree topologies under Lambda=1.0 and 0.0 indicated at right. E) Logio K [(BLOMBERG et al. 2003). Median values indicated by thick line; boxes include middle second and third quartiles of the data; whiskers extend to 1.5x the interquartile range of the data (~ 2 st. dev.).

Carboniferous and Early Permian of western Spitsbergen. The rugose corals (several dozen of specimens) collected on Kruseryggen (Hornsund area) and Polakkfjellet (Wedel Jarlsberg Land) hills and in Linnédalen (Grenfjorden area) valley (Fig. 1) are the base for my conclusions. Regarding rugose corals morphological specificity and their appearance in different places, the heterogeneity biostratinomic process and ecological conditions are possible to analyze. The mentioned areas present broad sedimentary environments and allow a nearly complete taphonomic analysis including almost all processes that happened during organism transfer from biosphere to ithosphere. Furthermore considering the fact, that the polyps occupy the highest part of skeletons only, hese animals are very useful for reconstructing processes that occurred in their life time. According to RODRIGUEZ (2004), the skeletons of those organisms might have been subjected to the influence of biotic and abiotic environmental factors shortly after their creation, changing original structures of the skeletons just before the death of the polyps. Consequently to the analysis of collected material the answer to the problem which changes have to be considered as ecological and which as biostratinomic becomes possible. Due to he small number of studies of the taphonomy of rugose corals in general (FEDOROWSKI 2003, RODRIGUEZ 2004), the results of my research could provide essential contribution to the understanding of the condition of fossil material. FEDOROWSKI, J. (2003): Some remarks on diagenesis of rugose coral skeletons. - Geologos, 6: 89-109. RODRIGUEZ, S. (2004): Taphonomic alterations in upper Viséan dissepimented rugose corals from the Sierra del Castillo unit (Carboniferous, Cordoba, Spain). - Palaeogeography, Palaeoclimatology, Palaeoecology, 214: 135-153.

Fig. 1: Facies model for the whole Frasnian platform (A) and for the carbonate mound (B); with facies distribution and main settings and corresponding stromatoporoid distribution (growth shape and type of stromatoporoid). and mound environments present i UUs area. Comparable facies were observed in the carbonate platform and in the mounds (Fig. 1). Although the mounds and platform are independent, similar stromatoporoids are observed in similar facies in each, indicating a strong paleo-environmental control. From the more distal to the more proximal, facies are: (1) outer platform or off-mound (shales, crinoidal packstones); (2) outer intermediate platform or deep mound (muddy facies with crinoids and reef-builders); (3) inner intermediate platform or shallow mound (muddy facies with algae) and (4) inner restricted platform or mound (laminites, mudstones, paleosols).

Fig. 2: Description of the main stromatoporoid morphologies and their distribution on the platform in relation to the substrate, biostrome and environment. Sti. = Stictostroma, StA. = Stachyodes australe and pf = platform. Stromatoporoid growth forms seem to be related mostly to environmental parameters but there is also some taxonomic control (Fig. 2 and DA SILVA et al. 2011 a and b).

Fig. 1: CL and SEM pictures, organization of the spicules and shape. Left: Large spicules organized as a perpendicular network in CL, with numerous small spicules. Right: Schematic sketch. The stromatoporoid skeleton is cassiculate with locally dominant coenosteles or coenostromes and with a melanospheric microstructure. The spicules are of two size ranges (Fig. 1), the large ones are ranging between 500 to 2000 um long and the small ones are 50 to 100 um long. They have a simple structure, styles (monoaxons), are circular and no axial canal is present, due to diagenetic processes (Fig. 1). Observed shapes are straight or slightly curved styles or strongyles. The spicules are organized as followed: they are commonly enclosed in the skeleton and are intramural. They are relatively closely packed and arranged as a perpendicular network (Fig. 1) or plumos following the main skeleton.

Fig. 2: Comparison of Newellia mira (WooD et al. 1989) and Euzkadiella erenoensis (REITNER 1987) with the stromatoporoid presented in this paper from La Boverie quarry. The type of spicules and their arrangement is relatively similar but their size is strongly different with spicules 10 times bigger in our specimen. The arrangement and type of spicule is relatively close to the observations made in the Upper Carboniferous haplosclerid demosponge “Newelia” mira (WOOD et al. 1989) (Spongonewellia sensus OZDIKMEN 2009) and Lower Cretaceous Euzkadiella erenoensis (REITNER 1987) but the size of the spicules in the Devonian specimen is ten times bigger (Fig. 2).

Fig. 1: stratigraphic distribution and proposed phyletic lineage for Dorlodotia and related genera. Tournaisian smal. solitary corals (Corphalia ?, Caninia ?) are tought to gave rise to fasciculate genera by budding during the Lates' Tournaisian. One group gave rise to acolumellate Dorlodotia (D. pseudovermiculare and Asian species) and questionalbly to Kwangsiphyllum. Another group seems to evolved in columellate Dorlodotia (D. briarti and close species). The latter purchased a cerioid trend during the Middle Viséan (Livian), giving rise to Ceriodotia. Coral zones and substages after Pory et al. (2006).

Morphologically and asexually specific colonial Rugosa were recovered from the Early to Middle Carboniferous (Serpukhovian to late Bashkirian) of the Akiyoshi Terrane of southwest Japan. Individual corallites are small (ca. 1.7 mm in diameter) and occur as uniserial fasciculate and phaceloid growth forms with a deep calice. However, they contain mos major and minor septa, tabulae, and columella. manner, even given the structural constraints o of the constituents essential to the Rugosa, including wa In addition, each component occurs in a rather remarka f being rugose corals. That is, the walls are extremely dila ls, ble ed with the fibrous lining facing inward, occupying up to half of the corallite interior and thereby prohibiting the formation of dissepiments; major and minor septa occur alternate densely packed within corallites; tabulae are s parse and near-horizonta ; and the columella is represen y, although they are occasionally ed by the axial elongation of the cardinal septum (Fig. 1). Parricidal increase is solely by dichotomous branching (division). In bipartite increase, parent corallites always provide their descendants with dividing walls on a cardinal-counter plane (bilateral p ane) by an axial connec ion of the cardinal septa and he (opposite) counter septa. For structural reasons, offset corallites make the best use of parental skeletons, in a stable manner (Ezaki 2004). The remarkable integration of all these components culminates in somew unbalanced, rather than simple, corallite characteristics, thereby justi genus. hat fying the establishment of a new It is remarkable that similar corals have been reported from the initial stages of both rugosan (e.g., Late Ordovician Modesta prima TCHEREPNINA 1962) and scleractinian diversification (e.g., Triassic Zardinophyllum zardini MONTANARO-GALLITELLI 1975 and Pachydendron microthallos CUIF 1975), when spatial competition for attachmen earlier in Pant hallassa than elsewhere, following the Late remained limited. Similarly, the construction of the Akiyoshi organic reef complex occurred Devonian extinction event (e.g., OTA 1968; NAGAI 1985; EZAKI et al. 2007). These mutually similar corals are commonly characterized by morphologies that include thick walls, distinct septa, and simple columellas. However, the present Carboniferous genus is phylogenetica ly unrelated to the Ordovician Modesta, because the former shows a diffuso-trabecular, septal fine structure that is characteristic of the Carboniferous and Permian Rugosa (KATO 1963). Such similarity may have resulted from convergence. The Akiyoshi Terrane is famous for the occurrence of endemic rugose corals represented by pseud constructional opavonids (KATO & MINATO 1975). It is probable

Additionally, geochemical analyses (5180, 6'°C) were realized on oyster shells associated to the corals. The results indicate that the mean values of paleotemperatures were around 22°C and it represents optimal temperatures for zooxanthellate corals. However, considering the paleoenvironmental conditions and the paleoecological assemblage, the corals of the Isle of Skye are regarded as having belonged to an extreme ecosystem.

Fig. 1: Dorlodotia sokolovi (DOBROLYUBOVA 1958): specimen PIN 705/161, holotype, showing strong variability in axial structures and tabularium; a - transverse section, b, c - longitudinal sections. Dinantian, Brigantian, Mikhailov horizon, north-western part of the Moscow Basin, 50-60 km N. of the town of Borovichi. x 1.5.

Fig. 1: Lonsdaleia (Actinocyathus) subtilis (DOBROLYUBOVA 1958): specimen PIN 705/646; 1a - transverse section, x2; 1b - transverse section showing biform morphology of tabularium, x5; 1c - longitudinal section showing biform morphology of tabularium, x5; Lower Serpukhovian, Tarusa horizon, north-western part of the Moscow Basin, Retesha River 60 km northeast of the town of Boksitogorsk. Fig. 2: Lonsdaleia (Actinocyathus) subtilis (DOBROLYUBOVA 1958): specimen PIN 705/184; longitudinal section showing periaxial cone on left side of axial column, x5. Lower Serpukhovian, Tarusa horizon, north-western part of the Moscow Basin, Tutoka River 60 km northeast of the town of Boksitogorsk. Abbreviations: PI, Position I of SUTHERLAND (1965); PII, Position II of SUTHERLAND (1965); pa, periaxial tabella; at, axial tabella; pc, periaxial cone. Scale bar = 5 mm.

Fig. 1. (A) Normalised diversity of all tabulate corals, and of the three families Favositidae, Michelinidae and Syringoporidae; error bars represent the confidence interval at 95%; St: Strunian, Has: Hastarian, Ivo: Ivorian, Moli: Molinacian, Li: Livian, As: Asbian, Bri: Brigantian, Mos: Moscovian, Kasi: Kasimovian. (B) Cluster showing the faunal similarities between the considered geographic units; node supports at 1000 bootstrap replicates. abulates. Favositidae are not significantly changing. Like the Michelinidae, they are not recorded after the Brigantian. The pattern indicates that the recognized Favositidae (Emmonsia, Squameofavosites, Sutherlandia) are conservative taxa. The small colonies live predominanty in deeper-water and also in muddy environments and, obviously, are less controlled by facies changes or sealevel changes than the two other families, which prefer carbonate environments. The differing diversity curves of the families also indicate a declining disparity during the later Mississippian. Communicate fasiculate taxa (Multithecoporidae) gain predominance in the Pennsylvanian of the western Palaeotethys.

Fig. 1: Surface of Thamnopora orthostachys with corallites sealed off by pseudopercula; Marmorbruch, Plabutsch

Fig. 1: Distinct types of thickening deposits in representatives of some monophyletic scleractinian families. A. Acroporidae (Acropora cervicornis (LAMARCK 1816)): A; side view of the branch, A7 SEM micrograph of septal surfaces showing shingle-like bundles of fibers (A3 -enlargement); B.Pocilloporidae (Pocillopora damicornis (LINNAEUS, 1758): B1 fragment of the branch, Bz SEM micrograph of a septal surface covered with microtuberculate texture (B3 . enlargement); C. Flabellidae (Flabellum chunii MARENZELLER 1904): C; Distal view of a coralum, C2 septum covered with fibers arranged in thin scale-like units (C3- enlargement); D. Micrabaciidae (Stephanophyllia complicata MOSELEY 1876): D; Distal view of a coralum, D2 SEM micrograph of thickening deposits composed of irregular meshwork of small fiber bundles, D3 FESEM close-up on the bundles formed by extremely thin and short parallel fibers.

This contribution focuses on her coral and archeocyathid research, and her contribution to our Association for the Study of Fossil Cnidaria and Porifera. Her coral studies started with the collection of a Carboniferous fauna from Mundubbera, 300 km northwest of Brisbane, when visiting a friend following her graduation. She began a detailed study of this fauna in Brisbane.

Although probably sighted by early Portuguese, Spanish, Dutch and French navigators before 1770, it was Captain James Cook’s description and oceans that afforded the fascination with the GB describing it as: ’a wall of Coral Rock rising all mo large waves of vast Ocean meeting wit mountains high’. With settlement of Aust charts o ralia in 1 R that fol st perpen itions car f the reef in his journal of his voyage across the southern owed. Cook saw it as a navigational hazard dicular out of the unfathomable Ocean .. . the h so sudden a resistance make a most terrible surf breaking 1788, char included the reefs of the GBR; many of these exped ing of the coastline became essential and this ried naturalists. The first geologists to visit the reef was J.B. JUKES onboard the ‘Fly’ and in his two volume narrative of the voyage published in1847, provided the first interpretation of the structure of he GBR ( Fig. 1). geolo g Fam aren I See Sw re ical understanding of the GBR. Following the end of WW1, there was a surge in intetrest in the GBR, and H.C. RICHARDS, professor o: geology at the University of Queensland established the Grea encouraging scientific research on the GBR. RICHARD’S aim was to that end, planned to drill several holes across its northern, central and sout were completed, one in the north on Mic results were published by RICHARDS & HILL haelmas Cay off Cairns 1942). In 1957, a petroleum exploration wel Wreck Island to the north of Heron Island. The three wells had similar stratigraphies wit reefal material overlying a thinner sequence of foraminiferal carbonates and silicastics, and thicker sequence of marine and terresria he distinguish six units within t Pliocene/ Pleistocene boundary within erosional remnant of reefal developmen shelf the lowest part of reefal material was Pliocene. he reefal section, separa The Heron Island core was re-examined by Barrier Reef Committee with the goal o: o understand the evolution of the reef, anc hern parts. By 1937, two well: and the other at Heron Island in the south was drilled or h 100 - 150m o: in turn a muct sediments. Foraminiferal studies of the cores suggested tha’ P.G. FLOOD, and ed by disconformities with the dest unit (FLOOD 1993). If each unit is in during successive high stands, Heron Reef is in the order of 500ke old, the basal reefal unit corresponding to high stand of isotope stage 13. erpreted as the

Database, or links to specimen repositories), increased functionality of an online peer-review system, extension of the system to species-level name, and potential for migration to alternative platforms.

Fig 1.: Completeness of taxonomic information in corallosphere.org. Numbers of taxa for which information ha been contributed for several categories of information. Proportions of completed taxa are indicated in parenthese: The numbers are tabulated for all taxa, for all genera and subgenera, and for all genera and subgenera current! considered to be available and valid.

Fig. 1: Turnover rates for reef-coral species estimated using the collections of Cenozoic fossil corals from Indonesia in the collections of NCB Naturalis. Estimates are sub-epochs bins using weighted methods (JOHNSON & JAcKSON 2000). A. Species richness including both range-through (light shading) and observed (dark shading) richness within each bin, B. the number of samples with age assignments crossing the bin, C. Numbers of first occurrences, and D. last occurrences within each bin. Analysis of specimen-based compilations of reef-coral species occurrences indicate widely differing Late Oligocene to Recent histories of coral reef ecosystems in Southeast Asia and the Caribbean. Caribbean reef ecosystems were altered by regional extinction during the Oligocene/Miocene and_ the Pliocene/ Pleistocene (BUDD 2000; KLAUS et al. 2011). The Oligocene/ Miocene extinction was associated with the collapse of reef building in the region, but contrary to expectations, the Pliocene/Pleistocene extinction is associated with regional reef recovery (JOHNSON et al. 2008). The depauperate extant Caribbean biota includes survivors of this extinction, and very few new species have appeared since. Pl ambcowes: dee Linco faatliklknawsns wasceesl TOC Atbwdlwaee aacel aemwediaemn wise: sranuweanl Bex eau: aba bex cc lbamcel “Eves These analyses suggest that in Southeast Asia, the Late Oligocene and Early Miocene is an interval of increased diversification (Fig. 2) that coincides with an expansion in coral-reef

Fig. 2: Changes in the midpoint of ages assigned to coral samples from the collections of NCB Naturalis. New ages obtained after examination of associated larger benthic foraminifera. development in the region (WILSON 2008). No intervals of accelerated extinction have yet been discovered in the Southeast Asian Neogene, suggesting that the high diversity of the regional reef biota is a function of continuous diversification. These results suggest that the regional response of coral reef ecosystems to global environmental change is strongly modulated by regional historical factors. Attempts to understand long-term global patterns of diversity and ecosystem distributions are enhanced by analysis of variation at non-global scales.

Fig. 1: Map of the Carnic Alps with four localities indicated that represent Middle Devonian coral bearing units. (1) Unbedded limestone of the Devonian carbonate platform succeeded by Hochwipfel Formation (Carboniferous) at Forc. Monumenz near Marinelli Refuge, (2) Kellergrat Reef Limestone of the abandoned quarry at the trail #149 to Marinelli Refuge, (3) Amphipora Limestone outcropping in the meadow and wood below the northern wall of the Devonian carbonate platform of Mount Zermula, Lanza, (4) View of the Devonian carbonate platform succeeded by the Hochwipfel Formation which is bounded by fault with the Devonian limestone breccia levels of the Hoher Trieb Formation.

Fig. 2: (1) Within the massive limestone single specimens of Thamnopora are observed along trail #143 to Mount Hohe Warte, (2) Amphipora Limestone (photo was taken at Forc. Monumenz, near trail #143, north of Marinelli Refuge), (3, 4) Alveolites, rugose corals and branching stromatoporoids (both abandoned quarry at the trail #149 to Marinelli Refuge), (5, 6) Beds with Amphipora are alternating with rugose coral biostromes (Amphipora Limestone along the base of the northern wall of Mount Zermula at Lanza), (7, 8) Silicified tabulate (e.g. Heliolites) and rugose corals from limestone breccia levels of the Hoher Trieb Formation at Cadin di Lanza Parete between Zuc della Guardia and Mount Pizzul, Lanza.

Fig. 1: A, B. Large, tubular microeuendolithic filaments inside the skeleton of microsolenid coral. Filaments are arranged parallel to the coral growth direction. Lower Aptian, Rarau Mts. C-F. Corals from Upper Aptian-? Lower Albian , Padurea Craiului. Amphiastreid (C) and heterocoenid (D) from coral biostromes. E. Coral from Bacinella facies. F. Calamophylliopsis fotisaltensis from intercalation of sandy limestones. G-I. Dense, coral platestones. On I undetermined coral encrusted by coralline Sporolithon rude, peysossonneliacean Polyastra alba and microsolenid coral. Upper Aptian, Resita-Moldova Noua zone.

Fig. 1: Fauna distribution in the Kasimovian deposits of the Donskaya Luka (Volgograd region, Russia). For stratigraphy see GOREVA et al. 2009

a © See 1- 5. Bothrophyllum domheri (FOMICHEV), 1-2 - x 3, 3 - x 2, 4-5 - x 1,5. Specimen Sz-7-1. Donskaya Luka, Seleznev Ravine, Seleznev Fm., Locality 5, uppermost part. Khamovnikian Substage, Kasimovian Stage. 6-8. Bothrophyllum domheri (FOMICHEV). Neanic stages in the incomplete specimen Cz-1-2, x 3. Ibid. 9-11. Pseudotimania mosquensis (DOBROLYBOVA), x 3. Specimen Don- 1-4-2. Donskaya Luka, Section Don, Sukhov Fm., Locality 1, Krevyakinian Substage, Kasimovian Stage. 12-15. Gen. et sp. nov.1 12-14 x 3, 15 x 1, 5. Specimen D-1-4a. Donskaya Luka, Section Don, Sukhov Fm., Locality 1, Krevyakinian Substage, Kasimovian Stage. 16. Gen. et sp. nov.1 Late neanic stage. Specimen SZ-5-4, x 3. Donskaya Luka, Seleznev Ravine, Seleznev Fm., Locality 5, uppermost part. Khamovnikian Substage, Kasimovian Stage.

Fig. 1: The ranges of the rugose coral species from Yashui section. The approximate Visean/Serpukhovian boundary is according to the Foraminifers study of Wu et al. (2009). M. ARETZ, S. DELCULEE, J. DENAYER & E. POTY (Eds.) Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liége, August 19-29, 2011

To obtain a representative value for the arithmetic mean, only a low number of measurements is required (20-30), but in order to obtain representative values for the standard deviation, the coefficient of variation and the first interval more values are necessary (> 50). The results are compared to traditional methods by remeasuring published material. It is concluded that the application of systematic measuring should be extended to other species rich coral genera. Fig. 1: Screen shot of the program used to measure the dimensions of the corals (PaleoTax/Measure).

Fig. 1: Chaetetid monoculture at the base of reef framework, seen from underneath (chaetetids outlined to show contrast). Fig. 2: Colony of Caninostrotion (rugose corals). aN DE DD EE The 2.7 meters of reef facies is comprised of 3 repeating growth cycles. Biological succession appeared to occur within each of these 3 cycles. The base of each cycle is colonized by a monoculture of chaetetids. These chaetetid layers can be observed from underneath within the cave (Fig. 1). Contemporaneous to, or shortly after chaetetid growth, microbialites began encrusting the tops and interstitial space between the chaetetids. This initial framework created hard surfaces, suitable for coral nucleation, and colonies of Caninostrotion soon after began to take root, greatly adding to the framework (Fig. 2). During the main phase of reef growth, all reefal organisms, including skeletal metazoans, encrusters, bafflers, and mobile organisms, continued to appear throughout the section until the subsequent cycle begins with another chaetetid monoculture.

Fig. 1: Distribution of Early Jurassic corals in the SE Pamirs 4 ® a YU Jurassic sedimentation began on both sides of the uplift by deposition of two suites of transgressive conglomerates discordantly overlying Permo-Triassic sequences: the Darbazatash suite on the south and the northern Kizylbeless suite. In both zones, sedimentation was followed by deposition of carbonate suites provided with the same names as the zones: Ghurumdy suite and Mynhadjir suite. They are composed of limestones with diverse lithologies, in the Ghurumdy suite, with a Hettangian-Sinemurian age indicated by ammonites of the Schlotheimiidae. The lower part of Mynhadjir suite is considered to be of the Hettangian- Sinemurian age as well. The above suites are covered by suites Sedek and Zormynhadjir, composed of black, well striated limestones. In the lower Ghurumdy sub-suite, a well diversified coral fauna is known: the solitary forms Archaeosmilia, Cylismilia, phaceloid genera, Archaeosmiliopsis, Prodonacosmilia, Intersmilia, Proaplophyllia and lamellate colonial forms Eocomoseris (MELNIKOVA 1975, 1989, MELNIKOVA & RONIEWICZ 1976; MELNIKOVA et al. 1993). In the coeval lower part of the Mynhadjir suite, Cylismilia has been found. a’ 7 ; -_ we % ag a,

Fig. 1: A. Pseudopistophyllum woznikensis MORYCOWA, Upper Tithonian (exotic), Outer Carpathians (MORYCOWA 1974). B. Amphiastrea basaltiformis sensu KoBy, Upper Tithonian (exotic), Outer Carpathians (MORYCOWA 1964). C. Microsolena exigua Kosy, Tithonian, Carpathian Foreland. D. Thamnasteria concinna (GOLDFUuUss), Tithonian, Carpathian Foreland. E. Isastraea bernensis ETALLON, Tithonian, Carpathian Foreland.

Fig. 1: A) Pebble clast of an Acropora branch encased with a cavity in another colony of Acropora sp. lined with clypeotheca (arrows). B) Photograph of fused coral branch alive on the reef flat of Heron Reef. C) SEM image on a polished and etched section of large amount of thickening deposits in the broken branch. Hence, we have demonstrated that live coral branches produced during a disturbance event may come to rest on probable genetic clone colonies and become fused. The retention of branch fragments on colonies in high energy reef flat settings suggests an active role of coral polyps to recognise and fuse with each other. This ability may represent an adaptation to help heal damaged colonies where branches were broken, but not removed from the host colony. Such an adaptation may be important for protecting colonies from invasion by parasites and other benthos following disturbance events.

Fig. 1. Photographs of a section cut through an Acropora sp. sample collected from Moreton Bay, Australia. A) Numerous laterite pebbles contained within the corallum. B) Enlargement of one pebble contained within a cavity lined by clypeotheca as marked by arrows. Moreton Bay and rocky headlands along the Queensland coast. Recognition of stress-related coral morphology may aid identification and interpretation of environmental stress events in ancient and living coral reefs, providing both a management tool and a new data set for understanding the effects of climate change and human interference in reef environments.

mosquensis STUCKENBERG. Similar chaetetid biostromes are described in similar stratigraphic levels in the Moscow region and the USA (WEST & CLARK 1984).

Fig. 1. Stratigraphy of the Kiyasar section The authors studied corals in the Kiyasar section, which is located in Northern Iran and the eastern limit of Alborz Mountains (latitude N: 36 14'18", longitude E: 53 32'57"). During the Early Carboniferous time the Alborz Mountains were part of the Gondwana margin (BRENCKLE et al. 2009). The Mobarak Formation includes alternations of thin to thick-bedded limestone, dolomitic limestone with interbedded shale and dark marl. Facies analyses show that this formation is composed of shallowing upward cycles, which are deposited on carbonate ramp.

The peculiarity of the studied corals has their endemicity, appearing in a large number of new species of rugose corals. The absence of Syringoporidae and colonial rugose corals in the studied, which are found at that time in many paleogeographic regions of Asia (China (XU & PoTy 1997), Kuzbas, and Tien-Shan) is unusual and confirms the conclusions about the features of paleogeography of this region (BRENCKLE et al. 2009).

Fig. 1: Plot of natural logarithm of 210 Pb with depth for the four samples from the Sinularia pedestal collected at Nukubuco. ee eae oe M. ARETZ, S. DELCULEE, J. DENAYER & E. Poty (Eds.) Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liege, August 19-29, 2011

Fig. 1: Correlation between the Western European and the South Chinese coral zonations with regard to the Foraminifer zonation. The doted lines indicate the first appearances of the recorded colonial rugose coral genera. Their stratigraphic distributions are not traced here. HANCE, L., Hou, H. & VACHARD, D. (in press): Upper Famennian to Visean Foraminifers and some carbonate microproblematica from South China - Hunan, Guangxi and Guizhou. PoTy, E., ARETZ, M., Hou, H. & HANCE, L. (2011): Bio- and sequence stratigraphic correlations between Western Europe and South China: to a global model of the eustatic variations during the Mississippian. - Abstracts of the XVII International Congress on the Carboniferous and Permian, Perth, Australia. POTY, E., DEVUYST, F.-X. & HANCE, L. (2006): Upper Devonian and Mississippian foraminiferal and rugose coral zonation of Belgium and Northern France: a tool for Eurasian correlations. - Geological Magazine, 143: 829-857. PoTY, E. & Xu, S. (1996): Rugosa from the Devonian-Carboniferous transition in Hunan (SW-China). - Mémoires Institut Géologique Université de Louvain, 36: 89-139. Poty, E. & Xu, S. (1997): Systematical position of some Strunian and Lower Carboniferous Heterocoral-like colonial corals. - Boletin de la Real Sociedad Espanola de Historia Natural (Seccién Geoldgica), 91 (1-4): 99-106.

Fig. 1: Depositional model and reef zonation of the studied portion of the Upper Jurassic reef complex. The figure shows the distribution of the main reef components in relation to the reconstructed depositional profile. Reef zones correspond to different sub-environments defined by distinct abiotic characteristics, distinctive biotic assemblages and characteristic hydrodynamic regime. (modified after RUSCIADELLI et al. 2011). n the history of the Earth, the Late Jurassic is generally known to be a time when reefal activity was widely expanded (KIESSLING 2002; Woop 1999), with a greater diffusion and differentiation of reefs in the Tet hys realm (e.g. CECCA et al. 2005; LEINFELDER et al. 2002). On the basis of their biotic composition and their paleogeographic setting, Upper Jurassic reefs have been subdivided into distinctive types of reef complexes (CREVELLO & HARRIS 1984; LEINFELDER et al. 2002; SCOTT 1988). Mixed coral- stromatoporoid ree fs dominate Isolated Intra-Tethys platform margins, whereas in the North Tethys/North Atlantic reefs, corals largely out-competed stromatoporoids (see LEINFELDER et al. 2002; 2005 for a review). Unlike other Up per Jurassic reefs, which have been the subject of numerous and detailed studies, Intra-Tethyan reefs have received little attention. Studies are in large part descriptive and only rarely contain sedimentological, taxonomical or paleoecological contributions. Recently RUSCIADELLI et al. (2011) have proposed an innovative zonation model for Upper Jurassic Intra-Tethys reef complexes. This model is based on excellent exposures in central Apennines (Italy) that allow the reconstruction of the reef profile across the Upper Jurassic platform margin. The zonation is revealed by the distribution of main reef builders (corals and calcified demosponges) and sedimentological characteristics along the reef complex (Fig. 1).

Fig. 1: Gregaria in Darwasophyllum sp. from the Etherington Formation. A- Group of individuals growing together. Note that the two corallites at the lower right seem to share structures. B- Close-up of figure A, showing stylolite (arrows), which produces the false impression of shared structures common to these neighbouring corallites. C- Numerous young corallites surrounding an adult corallite. None of them is an offset, but several are attached to the wall of the largest corallite.

af 7 The first coral beds occur in the upper part of the Betaina Formation, which is mainly siliciclastic, but shows some thin marly beds in its upper part. Those marly beds provided large in situ colonies of Siphonodendron sp. (-A coral bed, Fig. 2). This species shows similar dimensions to S. irregulare, but the number of major septa is similar to S. sociale. Near the top of the Betaina Formation, several beds containing corals have been identified (coral beds A- D). The coral assemblage here is dominated by Siphonodendron martini and S. sociale. The next assemblages are more diverse, containing both solitary (Axophyllum sp. and Palaeosmilia murchisoni) and colonial corals Siphonodendron martini and syringoporoids, coral beds E and F).

Fig. 1: Location and distribution facies in the Tiouinine reef. A.- Location of the Khenifra area. B.- Location of the Tiouinine reef in the Khenifra area. C.- Distribution of facies in the Tiouinine reef.

Fig. 1: Reconstruction of Darwin’s coral reef specimen exhibit and its likely relationship to his generalized reef transect for Cocos (Keeling) atoll (published in simplified form in DARWIN 1842). We infer that caption “2 and 3” refers to these two specimens of Millepora platyphylla HEMPRICH & EHRENBERG 1834.

How does Darwin's work at Cocos (Keeling) relate to ancient reefs? Around that time, Darwin made an intriguing and important sketch (CUL DAR 41.83, STODDART 1995) of how he envisaged a subsiding atoll’s growth through geological time. Although he never published a fair copy of this, his long footnote (1842, pp. 116-118) is conceptually related to his sketch (“I may take this opportunity of briefly considering the appearances, which would probably be presented by a vertical and deep section across a coral formation .... This is a subject worthy of attention, as a means of comparison with ancient coral strata.”).

Sig TN ORs TS) SEGNETE EST ee TRE eS a a, eae Platy coral assemblages, mainly common of Burdigalian to Serravallian age (11-20 Ma). Our observations suggest that the coral succession starts with very thin platy coral forms (1-10 mm) able to settle directly on soft sediments (Fig. 1A), or using fine sand grains, mollusks, or forams, as substrate to initiate growth. These initial stages are characterized by a high diversity, which is slowly replaced by a community dominated by few coral species that develop thicker and larger tabular colonies (Fig. 1B). Some of the most representative genera were Porites, Cyphastrea, Hydnophora, Pachyseris, Echinopora (Fig. 1C), Echinophyllia, and Leptoseris. Although scattered, some colonies of branching Porites and Acropora were also observed within the platy coral matrix. Platy coral communities could be interpreted as an adaptive response to extreme environmental conditions around the Kutai Basin: poor light levels in waters with high sedimentation rates (ROSEN et al. 2001; WILSON 2005). Fig. 1: Platy coral assemblages during the Miocene in East Kalimantan: (A,B) Section TF126 Serravallian (11.6-13.8 Ma), predominance of thin platy coral colonies at lower units (A) followed by the accumulation of thicker tabular coral colonies at upper units (B). (C) Section TF153, Burdigalian (16-20.4 Ma), showing a large platy colony of Echinovora sv.

Fig. 1: Schematic W-E profile across the Tabainout mound.

very shallow water carbonates changing cyclically from high- energy to low energy facies, thus biostromal in part. M. LECOMPTE was a scientist driven to succeed. He was a near personification of the ficticious but clearly Walloon, Belgian detective Hercule Poirot (Agatha Christie), a short, somewhat stout man in a dark suit and vest, a smoker who walked along with his hands clasped behind his back, an indefatiguable mind, incisive, with a ready sense of humor that was slight in the presence of strangers, but very well-developed and apparent when among friends. In addition he had a huge heart. One of my most vivid memories of M. LECOMPTE was him standing on the sidewalk in Prague in August of 1968, as invading tanks rumbled past us on the street. He had tears in his eyes and said to me, "This is just how it was in 1940." His compassion for the underdog was immense. This was a man who smiled easily when he was happy, was demanding in his professional life, enjoyed the presence of other scientists, truly enjoyed the café stop for beer after a day in the field, and was extremely kind to his friends. He was a man who rose from humble beginnings to earn international status as the leading student of his time in tabulate corals, stromatoporoid sponges and Devonian reef development in Belgium.

Fig. 1: Transverse section of Paleofavosites corallum with presumed annual couplets of zones based on varied spacing of tabulae, showing time equivalence of closely spaced tabulae (numbered dark bands) and the settling and growth of Tryplasma sp. associated with them. Field study of the Lower Silurian (Llandovery) Brassfield Formation exposed in abandoned quarries near Fairborn, Ohio, USA (KISSLING 1977) yielded a total of 274 tabular to columnar coralla of the tabulate species Paleofavosites prolificus. Fifty five (55) of these were from a hard-ground and high-energy sequence of strata forming the uppermost 30 cm of the formation. Of this collection (of 55), three exceptional Paleofavosites coralla contain symbiotic rugose corals of Tryplasma sp. partially or wholly imbedded within their skeleton, here reported for the first time. The rugosans are largely, but generally not totally immured within the favositid coralla, and as bioclaustrations (PALMER & WILSON 1988; TAYLOR 1990; TAPANILA 2005), permit further inferences on the paleobiology of both Tryplasma and Paleofavosites.

Fig. 1: Simplified log of the Pin Formation and the distribution of coral taxa. Historical units of HAYDEN (1904) are correlated to members which were proposed by SUTTNER (2007). Additional data based on this study are added here to the data provided by REED (1912).

Fig. 2: Rugose and tabulate corals from the Pin Formation. (1) Streptelasmatidae gen. et sp. indet., transverse section, Takche Member (unit P/10). (2) Favosites spitiensis, longitudinal section, Takche Member. (3, 4) Plasmoporella sp., transverse and longitudinal sections, Takche Member (unit P/13). (5) Halysites wallichi, transverse section, Takche Member. (6) Halysites? sp., transverse section, Mikkim Member (unit P/16).

Fig. 1: Unpublished drawings showing the relationships of different kinds of crystals in the wall of the genus Thecia MILNE-EDWARDS & HAIME 1849.

position of growth and it is unlikely that all corals sampled from this zone would be redeposited from older parts of the reef. Hence, this dating anomaly may correspond with a zone of increased marine diagenesis that appears to have affected the U-Th dating syst Such an increase in U-series age could result from U loss or 1 apparent increase in the ™°Th/*8U ratio and thus the calculated *°Th age from t However, in this case, the dated corals also contain high U values, making leaching of U an unlikely culprit. As this uppermost reef zone contains abundant microbialites (WEBB & JELL 1997) and the microbialites contain high Th concentrations rendering them unsuitable for U-series da microbialite contamination could be a problem. However, the dated corals suggesting against incorporation of a large amount of microbialite-derived Th. Hence, against expectation there appears to be direct evidence of Th open-system behaviour that a mobilisation and enrichment in his environment. It is likely that this zone o em so as to make corals appear to be too old. Th addition; either process would result in an he ratio would be too old. ing (Webb & Jell 2006) contain very little *°*Th, lowed preferential 2°Th f intense and unexpected diagenesis may reflect long-term suspension of corals immediately below the reef flat within the intertidal zone during the relatively long elevation since ~7 ka (LEWIS et a environment for long intervals of . 2007; YU & ZHAO 2010). Coral skeletons tha ime may be affected and have unreliable dates. ‘still-stand’ when local sea-level was maintained at or near its current occur in this ‘still-stand’ Shallow reef cores are only very rarely collected from closely spaced transects that can identify aggradation versus progradation ratios and many reef cores have only limited numbers of U-series dates in vertical sequence. Hence, zones of anomalous dates may not be recognised in some cases and some coral dates previously used for refining sea level curves, reef aggradation rates and for documenting reef growth models could be affected. Similar problems could exist for older corals obtained from current active reef flats. Hence, although the processes that might be responsible for preferential *°Th uptake in coral skeletons are under investigation, recognition of the potentially significant impacts for both dating and environmental proxies of the ‘still-stand’ diagenetic zone in ancient and modern coral reefs is critical.

Fig. 1: Results of discriminant analysis of massive Devonian phillipsastreid rugosans / canonical plot / 929 records, classified into 9 “genera” / analysis is based on 22 measurements or counts for each record (see WRZOLEK 2007) Among the massive phillipsastreid genera analyzed, the most outstanding, but also dubiously phillipsastreid, is the Famennian Sudetiphyllia FEDOROWSKI 1991, and then follow Smithicyathus ROZKOWSKA 1980, and Pachyphyllum MILNE-EDWARDS & HAIME 1851. The remaining genera: Chuanbeiphyllum He 1978, Frechastraea SCRUTTON 1968, Medusaephyllum ROEMER 1855, Phillipsastrea D’'ORBIGNY 1849 (sensu Ph. hennahii species group: WRZOLEK 2005), Phillipsastrea ananas species group and Scruttonia CHEREPNINA 1974 form a tight agglomeration, with abundant intermediate morphologies, and thus defy simple “statistical” discrimination, ie. if all characters analyzed are given equal weight.

ls ee ee: Dios ii hii: aia iia a As for numbers of publications there is a significant decrease during the last fifteen years (Fig. 1). In the beginning there was a lucky time with about 850 publications in the years 1971-1975, then 1015 in the years 1981-1985. On average, there were from 170 to 200 articles each year. The 1991-1995 interval marks the beginning of falling numbers, caused, among others factors, by a “significant decline in the size of the workforce” (SANDO 1997: 27). Also analysis of details shows negative trends in all our “publication” (if not research) areas: both thematical and geographical. As it seems from the preliminary analysis of our database, the negative trend has been slightly delayed (by 5 or 10 years) by numerous East-Asian (Chinese and Japanese) publications, but also this group of papers is in numerical decline now.

Fig. 1: A: Koutaliform auriculae at the second cycle of septa in transverse section in Heliocoenia sp. (Middle Oxfordian, Sorcy, Meuse, France). First cycle ornamented by rhopaloid or claviform sections of auriculae. B: Hastiform auriculae at the first cycle of septa in transverse section in Pseudocoenia sp. (Middle Oxfordian, Dompcevrin, Meuse, France). C: Flabelliform auricula at the second cycle of septa in Ironella rutimeyeri (Middle Oxfordian, Dompcevrin, Meuse, France). Third cycle rhopaloid/claviform or lanceolate in transverse section. D: longitudinal section of flabelliform auriculae of the same species.

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95. ARETZ, M. & HERBIG, H.-G. (2008): Microbial-sponge and microbial-metazoan buildups in the Late Viséan basin-fill sequence of the Jerada Massif (Carboiferous, NE Morocco). -In: ARETZ, M., HERBIG, H.-G. & SOMERVILLE, I.D. (Eds.) Carboniferous Platforms and Basins. Geological Journal, 43 (2-3): 307-336.
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105. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
106. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ ELIAŠOVA, H. (1975): Sous-ordre Amphiastraeina Alloiteau, 1952 (Hexacorallia) des calcaires de Štramberk (Tithonien, Tchécoslovaquie). -Časopis pro mineralogii a gelogii, 20: 1-23.
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114. KOŁODZIEJ, B. (2003): Scleractinian corals of suborders Pachythecaliina and Rhipidogyrina: Discussion on similarities and description of species from Štramberk-type limestones, Polish Outer Carpathians. -Annales Societatis Geologorum Poloniae, 73, 193-217.
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124. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
125. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
126. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
127. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ 112 by M. COEN and H.H. TSIEN and previously stored in the Geological Institut at Louvain-la-Neuve were moved to Brussels. Carboniferous corals are not so well-represented in collections of the RBINS contrary to their Devonian counterparts. As for the Belgian material, the collection of L. G. de KONINCK (1809-1897) comes mainly from the Tournaisian of Tournai and the Viséan of Visé. Some of these specimens were revised by POTY (1981) who also investigated some rugose corals collected by E. DUPONT and F. DEMANET. Finally, the Devonian and Carboniferous corals collected by CHARLES (1933) in Anatolia (Turkey) are also curated at the RBINS though his study was carried out at the Liège University. Of course, the types and illustrated specimens of all the papers mentioned in the paragraphs about the RBINS are housed in this institution.
128. BOLAND, K. (2002): Etude des Tétracoralliaires des couches de transition de la limite Tournaisien/Viséen en Europe occidentale. -Unpublished PhD thesis, Liège University, Liège, 390 pp.
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187. VERSEVELDT, J. (1971): Octocorallia from north-western Madagascar (Part II). Zool Verhandelingen Leiden, 117: 1-73. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
188. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
189. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ DENAYER, J. & POTY, E. (2010): Facies and palaeoecology of the upper member of the Aisemont Formation (Late Frasnian, S. Belgium): an unusual episode within the Late Frasnian crisis. -Geologica Belgica, 13: 197-212.
190. GODEFROID, J. & HELSEN, S. (1998): The last Frasnian Atrypida (Brachiopoda) in southern Belgium. -Acta Palaeontologica Polonica 43: 241-272.
191. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
192. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
193. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________
194. MOTTEQUIN, B. (2008a): New observations on Upper Devonian brachiopods from the Namur-Dinant Basin (Belgium). - Geodiversitas 30: 455-537.
195. MOTTEQUIN, B. (2008b): Late Middle and Late Frasnian Atrypida, Pentamerida, and Terebratulida (Brachiopoda) from the Namur-Dinant Basin (Belgium). -Geobios 41: 493-513.
196. MOTTEQUIN, B. (2008c): Late middle Frasnian to early Famennian (Late Devonian) strophomenid, orthotetid, and athyridid brachiopods from southern Belgium. -Journal of Paleontology 82: 1052-1073.
197. MOTTEQUIN, B., MARION, J.-M. & POTY, E. (2011): Preliminary data on Early and Middle Famennian (Late Devonian) rugose and tabulate corals from southern Belgium. -Kölner Forum für Geologie und Paläontologie (this volume).
198. POTY, E. (1999): Famennian and Tournaisian recoveries of shallow water Rugosa following the late Frasnian and late Strunian major crises, southern Belgium and surrounding areas, Hunan (South China) and the Omolon region (NE Siberia). -Palaeogeography, Palaeoclimatology, Palaeoecology, 154: 11-26.
199. POTY, E. & CHEVALIER, E. (2007): Late Frasnian phillipsastreid biostromes in Belgium. -In ÁLVARO, J.J., ARETZ, M. BOULVAIN, F., MUNNECKE, A., VACHARD, D. & VENNIN, E. (Eds.), Palaeozoic Reefs and Bioaccumulations: Climatic and Evolutionary Controls. Geological Society, London, Special Publications 275: 143-161.
200. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
201. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
202. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________
203. CECCA, F., GARIN, M., MARCHAND, D., LATHUILIERE, B. & BARTOLINI, A. (2005): Paleoclimatic control of biogeographic and sedimentary events in Tethyan and peri-Tethyan areas during the Oxfordian (Late Jurassic). -Palaeogeography, Palaeoclimatology Palaeoecology, 222: 10-32.
204. CREVELLO, P.D. & HARRIS, P.M. (1984): Depositional models for Jurassic reefal buildups. -In: VENTRESS,W.P.S., BEBOUT, D.G., PERKINS, C.H. (Eds.), The Jurassic of the Gulf Rim: Gulf Coast Section SEPM Foundation, Third Annual Research Conference Proceedings: 57-102.
205. KIESSLING,W. (2002): Secular variations in the Phanerozoic reef systems. -In: KIESSLING, W., FLÜGEL, E. & GOLONKA, J. (EDS.), Phanerozoic Reef Patterns. SEPM Special Publication, 72: 625-690.
206. LEINFELDER, R.R., SCHLAGINTWEIT, F., WERNER, W., EBLI, O., NOSE, M., SCHMID, D.U. & HUGHES, G.W. (2005): Significance of stromatoporoids in Jurassic reefs and carbonate platforms-concepts and implications. -Facies 51, 287-325.
207. LEINFELDER, R.R., SCHMID, D.U., NOSE, M. & WERNER, W. (2002): Jurassic reef patterns. The expression of a changing globe. In: KIESSLING, W., FLÜGEL, E. & GOLONKA, J. (EDS.), Phanerozoic Reef Patterns. SEPM Special Publication, 72: 465-520.
208. PREVER, P.L. (1909): Coralli giurassici del Gran Sasso d'Italia. -Atti della Reale Accademia delle scienze di Torino, 44: 986-1001.
209. RUSCIADELLI, G., RICCI, C. & LATHUILIÈRE, B. (2011): The Ellipsactinia Limestones of the Marsica area (Central Apennines): A reference zonation model for Upper Jurassic Intra-Tethys reef complexes. -Sedimentary Geology, 233: 69-87.
210. SCOTT, R.W. (1988): Evolution of Late Jurassic and Early Cretaceous reef biotas. -Palaios, 3: 184-193.
211. WOOD, R.A. (1999): Reef Evolution. Oxford University Press, Oxford, p. 414. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
212. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
213. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________
214. COCKE, J.M. (1970): Dissepimental rugose corals of Upper Pennsylvanian (Missourian) rocks of Kansas. - Paleontological contributions of the University of Kansas, 54: 1-67.
215. FEDOROWSKI, J. (1980): Some aspects of coloniality in corals. -Palaeontology, 25 (3-4): 429-437.
216. HERITSCH, F. (1936): Korallen der Moskauer-Gshel und Schwagerinen Stufe der Karnischen Alpen. -Palaeontographica, 83: 99-162.
217. MINATO, M. (1955): Japanese Carboniferous and Permian corals. -Journal of the Faculty of Science, Hokkaido University, 9(2): 1-202.
218. MINATO, M. & KATO, M. (1975): Geyerophyllidae Minato, 1955. -Journal of the Faculty of Science, Hokkaido University, Series 4, 17: 1-21.
219. PYZHYANOV, I.V. (1966). Nekotorye predstaviteli Rugosa iz nizhne-permskikh otlozhenyi severnogo Pamira. -Trudy Upr. Geol. Tadzhikistan SSR, 2: 265-297.
220. RODRÍGUEZ, S. (1985): The taxonomic status of the geyerophyllid corals. -Acta Geologica Polonica, 35 (3-4): 277-288. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
221. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
222. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ 3) Occurrence of the genera Lonsdaleia and Actinocyathus that have never been recorded in the northern basins from Morocco or in Sierra Morena (SW Spain) (SAID et al. 2007;ARETZ 2010).
223. Abundance of the genus Kizilia in Viséan beds. This genus is common in the Serpukhovian, but has been rarely recorded in the Upper Viséan (POTY 1981).
224. Late occurrence of the genus Tizraia, which is common in the lower Brigantian from the Azrou- Khenifra Basin (SAID et al. 2007; RODRÍGUEZ et al. 2010), but in the Tindouf Basin occurs first in the late Brigantian. The differences with assemblages from Northern Morocco and SW Spain could be explained by palaeogeography, but assemblages from Djebel Ouarkziz Formation show higher similarities with those from NW Europe (POTY 1981; MITCHELL 1989; ARETZ 2002; RODRÍGUEZ & SOMERVILLE 2007). Alternatively, the differences in the assemblages could be explained by ecologic factors; the succession in the Djebel Ouarkziz Formation shows some similarities with the successions described from the Brigantian in the British Isles (main intervals of shales with limestone intercalations), but are very different from the successions in SW Spain (CÓZAR & RODRÍGUEZ 1999) and North Morocco (SAID et al. 2007; ARETZ & HERBIG 2008; ARETZ 2010), where the formations contain large mud mounds.
225. ARETZ, M. (2002): Habitatanalyse und Riffbildungspotential kolonialer rugoser Korallen im Unterkarbon (Mississippium) von Westeuropa. -Kölner Forum für Geologie und Paläontologie, 10: 1-155.
226. ARETZ, M. (2010): Rugose corals from the upper Viséan (Carboniferous) of the Jerada Massif (NE Morocco): taxonomy, biostratigraphy, facies and palaeobiogeography. -Palaeontologische Zeitschrift, 84 (3): 323-344.
227. ARETZ, M. & HERBIG, H.-G. (2008): Microbial-sponge and microbial-metazoan buildups in the late Viséan basin-fill sequence of the Jerada Massif (Carboniferous, NE Morocco). -In: ARETZ, M., HERBIG, H.-G. & SOMERVILLE, I.D. (Eds.) Carboniferous Platforms and Basins. Geological Journal, 43 (2-3): 307-336.
228. CONRAD, J. (1972): L'age et les modalités de la regresión carbonifère au bord nord du Bassin de Tindouf. -Compte Rendu Academie des Sciences Paris, 274: 1780-1783.
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230. MAMET, B., CHOUBERT, G. & HOTTINGER, L. (1966): Note sur le Carbonifère du Djebel Ouarkziz. Etude du passage Viséen au Namurien d'après les Foraminifères. -Notes et Memoires du Service Géologique du Maroc, 27: 7-21.
231. MITCHELL, M. (1989): Biostratigraphy of Viséan (Dinantian) rugose coral faunas from Britain. -Proceedings of the Yorkshire Geological Society, 47: 233-247.
232. POTY, E. (1981): Recherches sur les Tétracoralliaires et les Hétérocoralliaires du Viséen de la Belgique. -Mededelingen Rijks Geologische Dienst, 35: 1-161.
233. RODRÍGUEZ, S. & SOMERVILLE, I.D. (2007): Comparisons of rugose corals from the Upper Viséan of SW Spain and Ireland: implications for improved resolutions in late Mississippian coral biostratigraphy. -In: HUBMANN, B. & PILLER, W.E. (Eds.), Fossil Corals and Sponges, Proceedings of the 9th International Symposium on Fossil Cnidaria and Porifera, Graz, 2003. Austrian Academy of Sciences, Schriftenreihe der Erdwissenschaftlichen Kommissionen, 17: 275-305.
234. RODRÍGUEZ, S., SOMERVILLE, I.D., SAID, I. & CÓZÁR, P. (2010): Tiouinine: un arrecife franjeante con la estructura preservada en el Misisípico de Marruecos. -III Congreso Ibérico de Paleontología, 265-268.
235. SAID, I., RODRÍGUEZ, S. & BERKHLI, M. (2007). Preliminary data on the coral distribution in the Upper Visean (Mississippian) succession from Adarouch area (NE Central Morocco). -In: HUBMANN, B. & PILLER, W.E. (Eds.), Fossil Corals and Sponges, Proceedings of the 9th International Symposium on Fossil Cnidaria and Porifera, Graz, 2003. Austrian Academy of Sciences, Schriftenreihe der Erdwissenschaftlichen Kommissionen, 17: 353-364.
236. WAGNER, R. H., WINKLER PRINS, C.F. & GRANADOS, L. F. (1985): The Carboniferous of the World, II Australia, Indian Subcontinent, South Africa, South America & North Africa. -Instituto Geológico y Minero, Madrid: 1-447. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
237. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
238. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ Fig. 1: Location and distribution facies in the Tiouinine reef. A.-Location of the Khenifra area. B.-Location of the Tiouinine reef in the Khenifra area. C.-Distribution of facies in the Tiouinine reef.
239. ADAMS, A. (1984): Development of algal-foraminiferal-coral reefs in the Lower Carboniferous of Furness, northwest England. -Lethaia, 17: 233-249.
240. ARETZ, M. (2002): Habitatanalyse und Riffbildungspotential kolonialer rugoser Korallen im Unterkarbon (Mississippium) von Westeuropa. -Kölner Forum für Geologie und Paläontologie, 10: 1-155.
241. ARETZ, M & HERBIG, H.-G. (2003): Coral-rich bioconstructions in the Viséan (Late Mississippian) of Southern Wales (Gower Peninsula, UK). -Facies, 49: 221-242.
242. COPPER, P. (1988): Ecological succession in Phanerozoic reef ecosystems: is it real? -Palaios, 3: 136-151.
243. NAGAI, K. (1985): Reef forming Algal Chaetetid boundstone found in the Akiyoshi Limestone Group, Southwest Japan. -Bulletin of the Akiyoshi-Dai Museum for Natural History, 20: 1-15
244. NEWELL, N.D. (1972): The evolution of reefs. -Scientific American, 226(6): 54-65.
245. RODRÍGUEZ, S, ARRIBAS, M.E., MORENO-EIRIS, E & DE LA PEÑA, J.A. (1994): The Siphonodendron Limestone of the Los Santos de Maimona Basin: development of an extensive reef-flat during the Viséan in Ossa Morena, Spain. -Courier Forschunginstitut Senckenberg, 172: 203-214.
246. SOMERVILLE, I.D. & RODRÍGUEZ, S. (2007): Rugose coral associations from the Upper Viséan of Ireland, Britain and SW Spain. -In: HUBMANN, B. & PILLER, W.E. (Eds.), Fossil Corals and Sponges, Proceedings of the 9th International Symposium on Fossil Cnidaria and Porifera, Graz, 2003. Austrian Academy of Sciences, Schriftenreihe der Erdwissenschaftlichen Kommissionen, 17: 329-351.
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248. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
249. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
250. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________
251. ARETZ, M. (2010): Rugose corals from the upper Viséan (Carboniferous) of the Jerada Massif (NE Morocco): taxonomy, biostratigraphy, facies and palaeobiogeography. -Paläontologische Zeitschrift, 84: 323-344.
252. ARETZ, M. & HERBIG, H.-G. (2008): Microbial-sponge and microbial-metazoan buildups in the late Viséan basin-fill sequence of the Jerada Massif (Carboniferous, NE Morocco). -In: ARETZ, M., HERBIG, H.-G. & SOMERVILLE, I.D. (Eds.) Carboniferous Platforms and Basins. Geological Journal, 43 (2-3): 307-336.
253. ARETZ, M. & HERBIG, H.-G. (2010): Corals from the Upper Viséan of the southern Azrou-Khenifra Basin (Carboniferous, Central Moroccan Meseta). -In: KOSSOVAYA, O. & SOMERVILLE, I.D. (Eds.), X Coral Symposium, St Petersburg. Palaeoworld, 19 (3-4): 294-305.
254. CÓZAR, P., VACHARD, D., SOMERVILLE, I.D., BERKHLI, M., MEDINA-VAREA, P., RODRÍGUEZ, S. & SAID, I. (2008): Late Viséan- Serpukhovian foraminiferans and calcareous algae from the Adarouch region (central Morocco). -Geological Journal, 43 (4): 463-485.
255. SAID, I, RODRÍGUEZ, S. & BERKHLI, M. (2007): Preliminary data on the coral distribution in the Upper Visean (Mississippian) succession from Adarouch area (NE Central Morocco). -In: HUBMANN, B. & PILLER, W.E. (Eds.), Fossil Corals and Sponges, Proceedings of the 9th International Symposium on Fossil Cnidaria and Porifera, Graz, 2003. Austrian Academy of Sciences, Schriftenreihe der Erdwissenschaftlichen Kommissionen, 17: 353-364.
256. SAID, I., RODRÍGUEZ, S., SOMERVILLE, I. D. & CÓZAR, P. 2011: Environmental study of coral assemblages from the upper Viséan Tizra Formation (Adarouch area, Morocco): implications for Western Palaeotethys biogeography. -Neues Jahrbuch für Geologie und Paläontologie, 260/1: 101-118.
257. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
258. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
259. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________
260. LECOMPTE, M. (1951): Les stromatoporoides du Dévonien moyen et supérieur du Bassin de Dinant. -Institut Royale des Sciences Naturelles Belgique, 116: 1-218.
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265. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
266. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
267. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ KERSHAW, S. (1987): Stromatoporoid-coral intergrowths in a Silurian biostrome. -Lethaea, 20: 371-380.
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269. LANG, J. & CHORNESKY, E.A. (1990): Competition Between Scleractinian Reef Corals-A review of mechanisms and effects: 209-257. -In DIBINSKY, Z. (Ed.), Coral Reefs' Ecosystems of the World. V. 25. New York: Elsevier.
270. PALMER, T.J. & WILSON, M.A. (1988): Parasitism of Ordovician bryozoans and the origin of pseudoborings. - Palaeontology, 39: 939-949.
271. TAPANILA, L. (2005): Palaeoecology and diversity of endosymbionts in Paleozoic marine invertebrates: Trace fossil evidence. -Lethaia, 38: 89-99.
272. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
273. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
274. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
275. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
276. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ 165 astonishingly, the coral polyps reacquired skeletons. This demonstrated experimentally the effects of acidification on coral survival and recovery, providing support for the "naked coral" hypothesis. The Middle Triassic delayed recovery of calcified corals through millions of years of geologic time is attributed to long lasting Early Triassic perturbation of the world's oceans in which "naked" corals sought out isolated refugia. These sorts of organisms surviving the extinction were effectively censored from the fossil record. In this form, coral may have survived for six million years. Their apparently sudden appearances constitute biocalcification responses to ameliorating conditions of ocean chemistry so it likely coincided with the point where biogenic CaCO 3 could be secreted. This was a different kind of long-term refugia and what I call the "naked Lazarus" effect. The "naked Lazarus" effect best explains the sudden appearance of corals and other anomalous aspects of the Middle Triassic recovery and it may apply to other organisms as well. Investigations to substantiate these conclusions must likely delve into lagerstätten, molecular biology, seawater experiments and metazoan physiology.
277. BOWRING, S. A., ERWIN, D. H. & ISOZAKI, Y. (1999): The tempo of mass extinction and recovery: The end-Permian example. -Proceedings of the National Academy of Sciences, 96: 8827-8828.
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280. FLÜGEL, E. (2002): Triassic Reef Patterns. -In: KIESSLING, W., FLÜGEL, E. & GOLONKA, J. (EDS.), Phanerozoic Reef Patterns. SEPM Special Publication, 72: 391-463.
281. FLÜGEL, E. & STANLEY, G.D. (1984): Reorganization, development and evolution of post Permian reefs and reef organisms. -Paleontographica Americana, 54: 177-186.
282. OLIVER, W.A., JR. (1996): Origins and relationships of Paleozoic coral groups and the origin of the Scleractinia. -In: STANLEY, G.D. Jr. (ed.), Paleobiology and Biology of Corals, V. 1: 107-135. Pittsburgh, Paleontological Society.
283. PAYNE J.L., LEHRMANN, D.J., WEI, J. & KNOLL, A.H. (2006): The pattern and timing of biotic recovery from the end- Permian mass extinction on the Great Bank of Guizhou, Guizhou Province, South China. -Palaios, 21: 63-85.
284. QI, W. & STANLEY, G.D. Jr. (1989): New Anisian corals from Qingyan, Guiyang, South China. -Lithopheric Geosciences, 1989: 11-18.
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286. SCRUTTON, C. (1999): Paleozoic corals: Their evolution and palaeoecology. -Geology Today, 15: 184-193.
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289. WEIDLICH, O. (2002): Permian reefs re-examined: extrinsic control mechanisms of gradual and abrupt changes during 40 my of reef evolution. -Geobios, 35:287-294.
290. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
291. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
292. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ Katian in units P/7 and P/13. Only few coral colonies were observed from the Silurian part of the sequence (P/16). REED (1912) described Streptelasma sp. aff. S. corniculum, Streptelasma sp. or Zaphrentis sp., Streptelasma? sp., Heliolites depauperata, Heliolites? sp., Lyopora? sp., Propora himalaica, Calapoecia? sp., Protaraea kanaurensis, Favosites spitiensis, Halysites catenularia var. kanaurensis, Halysites wallichi, Halysites sp. and listed the species of Plasmoporella from the Takche Member. Among them, the species, except for Streptelasma? sp., Heliolites depauperata, Lyopora? sp. and Plasmoporella sp., were ones that REED (1912) described from HAYDEN'S Horizon 6 as the Silurian species. According to REED (1912), (?)Llandoverian strata (Mikkim Member) yielded Favosites sp. cf. F. forbesi?, Favosites sp. cf. F. niagarensis?, Lindstroemia sp. and Calostylis dravidiana. Based on the present study of coral material collected from the type section we can confirm occurrences of following tabulate and rugose corals: Favosites spitiensis, Favosites sp., Plasmoporella sp., Halysites wallichi, Halysites? sp., Protaraea? sp., Proheliotidae? gen. et sp. indet., Calostylis? sp., Streptelasma sp., Streptelasmatidae gen. et sp. indet. Of them, Favosites sp. and Plasmoporella sp. occurred in the unit P/13.
293. Streptelasma sp., Streptelasmatidae gen. et sp. indet. and Halysites? sp. were found in the units P/8, 10 and 16, respectively. Others were collected in the well weathered rubble just below the section that derived from the Takche Member. This is a contribution to IGCP 591.
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300. SHEEHAN, P. M. (2001): The Late Ordovician mass extinction. -Annual Review of Earth and Planetary Sciences, 29: 331- 364.
301. SUTTNER, T. (2003): Die Pin Formation (Altpaläozoikum) von Muth, Spiti (Indischer Himalaya): Stratigraphie und Fazies. -Diploma thesis, University of Vienna, 1-80.
302. SUTTNER, T. J. (2007): The Upper Ordovician to Lower Silurian Pin Formation (Farka Muth, Pin Valley, North India) -A formal discussion and redefinition of its controversial type-section. -Acta Palaeontologica Sinica, 46: 460-465.
303. SUTTNER, T. J. & ERNST, A. (2007): Upper Ordovician bryozoans of the Pin Formation (Spiti valley, northern India). - Palaeontology, 50 (6): 1485-1518.
304. SUTTNER, T. J., LEHNERT, O., JOACHIMSKI, M. & BUGGISCH, W. (2007): Recognition of the Boda event in the Pin Formation of northern India based on new δ 13 C and conodont data. -Acta Palaeontologica Sinica, 46: 466-470.
305. WEBBY, B. D. (2002): Patterns of Ordovician reef development. -In: KIESSLING, W., FLÜGEL, E. & GOLONKA, J. (EDS.), Phanerozoic Reef Patterns. SEPM Special Publication, 72: 129-179.
306. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
307. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
308. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
309. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
310. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ BRANDANO, M., JADOUL, F., LANFRANCHI, A., TOMASSETTI, L., BERRA, F., FERRANDINI, M. & FERRANDINI, J. (2009): Stratigraphic architeture of mixed carbonate-siliciclastic system in the Bonifacio Basin (Early-Middle Miocene, South Corsica). -Field Trip Guide (FT13), 27th IAS International Meeting of Sedimentology, Alghero, Sardegna, Italy, 299-313.
311. FERRANDINI, M., GALLONI, F., BABINOT, J.F. & MARGEREI, J.P. (2002): La plate-forme carbonatèe burdigalienne de Bonifacio (Corse du Sud) : microfaunes et palèoenvironnements. -Revue Micropaléontologie, 45 (1): 57-68.
312. JOHNSON, M.E. (2006): Uniformitarianism as a guide to rocky-shore ecosystems in the geological record. -Canadian Journal of Earth Science, 43: 119-1147.
313. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
314. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
315. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________
316. CHEN, K.S., HSIEH, H.J., KESHAVMURTHY, S., LEUNG, J.K.L., LIEN, I.T., NAKANO, Y., PLATHONG, S., HUANG, H. & CHEN, C.A. (2011): Latitudinal gradient of morphological variations in Zebra coral Oulastrea crispata (Scleractinia: Faviidae) in the West Pacific. -Zoological Studies, 50 (1): 43-52
317. LAM, K.Y. (2000): Early growth of a pioneer recruited coral Oulastrea crispata (Scleractinia, Faviidae) on PFA-concrete blocks in a marine park in Hong Kong, China. -Marine Ecology Progress Series, 205: 113-121
318. SAKAI, K. (1998): Effect of colony size, polyp size, and budding mode on egg production in a colonial coral. -Biological Bulletin, 195: 319-325 _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
319. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
320. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ ABBINK, O.A., DEVUYST, F.X., GRÖTSCH, J., HANCE, L., VAN HOOF, T.B., KOMBRINK, H. & VAN OJIK, K. (2009): The Lower Carboniferous of key-well UHM-02, onshore The Netherlands, and implications for regional basin development. - European Association of Geoscientists and Engineers, 71th Conference and Technical Exhibition, June 8-11, Amsterdam, the Netherlands, extended abstracts W031, 5 p.
321. KOMBRINK, H. (2008): The Carboniferous of the Netherlands and surrounding areas; a basin analysis. -Geologica Ultraiectina, No. 294, Ph.D. thesis University of Utrecht, 184 p.
322. VAN HULTEN, F.F.N. & POTY, E. (2008): Geological factors controlling Early Carboniferous carbonate platform development in the Netherlands. -In: ARETZ, M., HERBIG, H.-G. & SOMERVILLE, I.D. (Eds.) Carboniferous Platforms and Basins. Geological Journal, 43 (2-3): 175-196.
323. VAN HULTEN, F.F.N. & POTY, E. (2009): Dinantian Reefs underneath the Netherlands. -European Association of Geoscientists and Engineers, 71th Conference and Technical Exhibition, June 8-11, Amsterdam, the Netherlands, extended abstracts W039, 5 p.
324. WEBER, L.J., FRANCIS, B.P., HARRIS, P.M. & CLARK, M. (2003): Stratigraphy, facies, and reservoir characterization -Tengiz Field, Kazakhstan. -In: AHR, W.M., HARRIS, P.M., MORGAN, W.A. & SOMERVILLE, I.D. (Eds.), Permo-Carboniferous Carbonate Platforms and Reefs, Joint SEPM Special Publication, 78 -American Association of Petroleum Geologists, Memoir, 83: 351-394.
325. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
326. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
327. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________
328. BUDD, A.F., STEMANN, T. & JOHNSON, K. (1994): Stratigraphic distributions of genera and species of Neogene to Recent Caribbean reef corals. -Journal of Palaeontology, 68: 951-997.
329. BUDD, A.F. & WALLACE, C.C. (2008): First record of the Indo-Pacific reef coral genus Isopora in the Caribbean region: two new species from the Neogene of Curacao, Netherlands Antilles. -Palaeontology, 51: 1187-1401.
330. JOHNSON, K. G. & KIRBY, M. X. (2006): The Emperador Limestone rediscovered: Early Miocene corals from the Culebra formation, Panama. -Journal of Paleontology, 80: 283-293.
331. STEMANN, T.A. (2004): Reef corals of the White Limestone group of Jamaica. -Cainozoic Research, 3: 83-107.
332. WALLACE, C.C., CHEN, C.A, FUKAMI, H. & MUIR, P.R. (2007): Recognition of separate genera within Acropora based on new morphological, reproductive and genetic evidence from Acropora togianensis, and elevation of the subgenus Isopora Studer, 1878 to genus (Scleractinia; Astrocoeniidae; Acroporidae). -Coral Reefs, 26: 231-239.
333. WALLACE, C. C., TURAK, E. & DEVANTIER, L. (2011): Novel characters in a conservative coral genus: three new species of Astreopora (Scleractinia: Acroporidae) from West Papua. -Journal of Natural History, 45: 1905-1924. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
334. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
335. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
336. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
337. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________
338. KAZMIERCZAK, J. (1971): Morphogenesis and systematics of the Devonian Stromatoporoidea from the Holy Cross Mountains, Poland. -Palaeontologia Polonica, 26: 1-150.
339. LECOMPTE, M. (1951): Les stromatoporoides du Dévonien moyen et supérieur du Bassin de Dinant. -Institut Royale des Sciences Naturelles Belgique, 116: 1-218.
340. LECOMPTE, M. (1952): Les stromatoporoides du Dévonien moyen et supérieur du Bassin de Dinant. -Institut Royale des Sciences Naturelles Belgique, 117: 219-360.
341. MAY, A. (2005): Die Stromatoporen des Devons und Silurs von Zentral-Böhmen (Tschechische Republik) und ihre Kommensalen. -Zitteliana B 25: 117-250.
342. MISTIAEN, B. (1980): Stromatopores du Givétien de Ferques (Boulonnais, France). -Bulletin du Muséum national d'Histoire naturelle 2, (4ème série): 167-257.
343. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
344. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
345. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________
346. MISTIAEN, B. (1988): Stromatopores du Givétien et du Frasnien de Ferques (Boulonnais -France). -In: BRICE, D. (Ed.), Le Dévonien de Ferques. Bas-Boulonnais (N. France). Collection Biostratigraphie du Paléozoïque, 7: 163-195.
347. PLOTNICK, R. E. (2007): SWOTing at paleontology. -American Paleontologist, 15 (4): 21-23.
348. SALERNO, C. (2008): Stromatoporen-Fauna, Fazies und Paläoökologie von Plattformkarbonaten aus dem Unter- Givetium der Eifel (Devon, Rheinisches Schiefergebirge). -Zitteliana, B 27: 3-129.
349. STEARN, C. W. (1966): The microstructure of stromatoporoids. -Palaeontology, 9 (1): 74-124.
350. STEARN, C. W. (1980): Classification of Paleozoic stromatoporoids. -Journal of Paleontology, 54: 881-902.
351. STEARN, C.W. (1999): Easy access to doubtful taxonomic decisions. -Palaeontologia Electronica, 2: 4 pp. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
352. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
353. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ 190 Comments on subspecies of Calceola sandalina Anthony WRIGHT 1 & Harald PRESCHER 2
354. LOTZE, F. (1928): Beitrag zur Kenntnis der Mutationen von Calceola sandalina (L.). -Senckenbergiana, 10: 158-169.
355. RICHTER, R. (1916): Zur stratigraphischen Beurteilung von Calceola (Calceola sandalina Lam. n. mut. lata und alta). - Neues Jahrbuch für Mineralogie, 1916/2: 31-46.
356. RICHTER, R. (1928): Fortschritte in der Kenntnis der Calceola-Mutationen. -Senckenbergiana, 10: 169-184.
357. WERNER, R. (1968): Calceola sandalina aus den Heisdorf-Schichten (Unter-Devon) der Eifel. -Senckenbergiana lethaea, 49: 575-580.
358. WRIGHT, A.J. (2001): A new Early Devonian operculate coral genus from eastern Australia. -Records of the Western Australian Museum, Supplement 58: 21-35.
359. WRIGHT, A.J. (2006): New genera of Early Devonian calceolide corals from Australia and France. -Palaeoworld, 15: 185- 193. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
360. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
361. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ 191 Soft taxonomy -case of Devonian phillipsastreid rugose corals Tomasz WRZOŁEK University of Silesia, Dept of Earth Sciences, ul. Będzińska 60, PL 41-200 Sosnowiec, Poland;
362. or/and its high phenetic plasticity. The other factor responsible may be small size of variability space analyzed. Among the massive phillipsastreid genera analyzed, the most outstanding, but also dubiously phillipsastreid, is the Famennian Sudetiphyllia FEDOROWSKI 1991, and then follow Smithicyathus RÓŻKOWSKA 1980, and Pachyphyllum MILNE-EDWARDS & HAIME 1851. The remaining genera: Chuanbeiphyllum He 1978, Frechastraea SCRUTTON 1968, Medusaephyllum ROEMER 1855, Phillipsastrea D'ORBIGNY 1849 (sensu Ph. hennahii species group: WRZOŁEK 2005), Phillipsastrea ananas species group and Scruttonia CHEREPNINA 1974 form a tight agglomeration, with abundant intermediate morphologies, and thus defy simple "statistical" discrimination, i.e. if all characters analyzed are given equal weight.
363. FEDOROWSKI, J. (1991): Dividocorallia, a new subclass of Palaeozoic Anthozoa. -Bulletin de l'Institut royal des sciences naturelles de Belgique, Sciences de la Terre, 61: 21-105.
364. PICKETT, J. W. (1967): Untersuchungen zur Familie Phillipsastreidae (Zoantharia rugosa). -Senckenbergiana lethaea, (1): 1-89.
365. SCRUTTON, C. T. (1968): Colonial Phillipsastraeidae from the Devonian of South-East Devon, England. -Bulletin of the British Museum (Natural History) Geology, 15 (5): 21-281.
366. WRZOŁEK, T. (2005): Devonian rugose corals of the Phillipsastrea hennahii species group. -Acta Geologica Polonica, (2): 163-185.
367. WRZOŁEK, T. (2007): A revision of the Devonian rugosan phillipsastreid genus Smithicyathus. -Acta Palaeontologica Polonica, 52 (3): 609-632.
368. _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
369. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
370. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ _________________________________________________________________________________________________________ Kölner Forum Geol. Paläont., 19 (2011)
371. M. ARETZ, S. DELCULÉE, J. DENAYER & E. POTY (Eds.)
372. Abstracts, 11th Symposium on Fossil Cnidaria and Sponges, Liège, August 19-29, 2011 _________________________________________________________________________________________________________ 202
373. Authors ADACHI, N. 6, 8
374. ARETZ, M. 10, 12, 35, 96, 100, 135
375. ASHOURI, A. 14 BADPA, M. 14
376. BAMBER, E.W. 44, 142 BATBAYAR, M. 15
377. BEGG, Z. 129 BERKOWSKI, B. 16 BERKYOVÁ, S. 73 BERNECKER, M. 18 BOEKSCHOTEN, G.J. 20 BOSELLINI, F.R. 21, 173, 180 BOULVAIN, F. 30, 32
378. BRANDANO, M., 173 BUCUR, I.I. 81
379. BUDD, A.F. 23 CAIRNS, S.D. 59
380. CASTRO, J.M. 99 CHANTRY, G. 25
381. CHWIEDUK, E. 27 COEN-AUBERT, M. 28, 111
382. COLLEN, J. 129 CORRADINI, C. 73 CORRIGA, M.G. 73
383. COZAR, P. 144, 147, 158 CRONIER, C. 127
384. DA SILVA, A.C. 30, 32
385. DARELL, J. 151 DEBRENNE, F. 71
386. DENAYER, J. 25, 34, 35, 37, 137
387. DEVLEESCHOUWER, X. 53 EZAKI, Y. 6, 8, 40, 70 157, 177
388. FALAHATGAR, M. 123
389. FEDOROWSKI, J. 42, 46 GOREVA, N. 86 GRETZ, M. 45
390. HECKER, M.R. 47, 49 HERBIG, H.-G. 51
391. HOLZER, P. 57
392. HUBERT, B.L.M. 53, 127 HUBMANN, B. 55, 59 IDAKIEVA, V. 80, 83
393. IVANOV, M. 80, 83 JANISZEWSKA, K. 59
394. JAOUEN, P.-A. 128 JELL, J.S. 61, 63, 119
395. JOHNSON, K.G., 65, 67, 155
396. KARIMOVA, F.S. 69, 154 KATO, M. 40, 70 KERNER, A. 71 KERSHAW, S. 30, 32 KHAKSAR, K. 14
397. KIDO, E. 73, 169 KISSLING, D.L. 162 KITAHARA, M. 59 KOLODZIEJ, B. 77, 80, 83 KOSSOVAYA, O. 86, 90
398. KRUSE, P.D. 92 LATHULIERE, B. 45, 140, 197 LAZAR, D. 77 LIAO, W. 94
399. LIN, W. 96 LIU, J. 2, 4 LÖSER, H. 98, 99
400. LORD, E.K. 100
401. MORYCOWA, E. 108, 151 MOSADDEGH, H. 123 MOTTEQUIN, B. 111, 113, 137 MOTUS, M-A. 115 MÜLLER, A. 51 NARDIN, E. 51 NGUYEN, H.H. 116 NIETO, L. 101
402. NOTHDURFT, L.D. 117, 119, 186 NOVAK, M. 90 OGAR, V. 121, 123 OPDEYKE, B.: 186 OSPANOVA, N.K. 125 PETITCLERC, E. 53
403. PINTE, E. 53, 127 PLUSQUELLEC, Y. 128 POHLER, S. 131 PONDRELLI, M. 73
404. POTY, E. 25, 37, 96, 111, 113, 135, 137, 139 PREAT, A. 53 PRESCHER, H. 190
405. PRICE, G.J. 119, 186 REITNER, J. 32 REMY, G. 128 RENEMA, W. 67
406. SASARAN, E. 77 SENTOKU, A. 157 SILVESTRI, G. 21 SIMONETTO, L. 73 SMITH, N.D. 23 SOMERVILLE, I.D. 143, 147, 158
407. SORAUF, J.E. 160, 162 STAKE, J.L. 199 STANLEY, G.D. JR 164 STEMANN, T.A. 166 STOLARSKI, J. 59, 167, 180 SUGIYAMA, T. 182 SUTTNER, T.J. 73, 169 TOMASSETTI, L., 173 TOURNEUR, F. 107, 175
408. UEDA, S. 177 VAN HULTEN, F.F.N. 178 VERTINO, A.V., 180 WALKER, S.E. 100 WANG, XD. 96 WEBB, G.E. 118, 120, 182, 184, 186 WEYER, D. 16, 90 WOLNIEWICZ, P. 188
409. WRIGHT, A. 190 WRZOLEK, T. 191, 194, 196
410. KÖLNER FORUM FÜR GEOLOGIE UND PALÄONTOLOGIE ISSN 1437-3246 alle Preise incl..
411. % MWSt.
412. HENZE, N. (1998): Kennzeichnung des Oberwürmlösses der Niederrheinischen Bucht. 38,--€
413. S., 61 Abb., 8 Tab., 1 Taf.
414. MESTERMANN, B. (1998): Mikrofazies, Paläogeographie und Eventgenese des crenistria-Horizontes 28,--€ (Obervisé, Rhenohercynikum). 77 S., 14 Abb., 8 Taf.
415. PREUSSER, F. (1999). Lumineszenzdatierung fluviatiler Sedimente. Fallbeispiele aus der Schweiz 20,--€ und Norddeutschland. 62 S., 48 Abb., 26 Tab.
416. BRÜHL, D. (1999): Stratigraphie, Fazies und Tabulaten-Fauna des oberen Eifelium (Mittel-Devon) 30,--€ der Dollendorfer Mulde/Eifel (Rheinisches Schiefergebirge). 155
417. S., 10 Abb., 1 Tab., 43 Taf.
418. SCHRADER, S. (2000): Die sedimentär-geodynamische Entwicklung eines variscischen Vorland- 28,--€ beckens: Fazies-und Beckenanalyse im Rhenohercynischen Turbiditbecken (Spätes Viseum, cd III).
419. S., 56 Abb., 3 Tab.
420. ZANDER, A.M. (2000): Vergleich verschiedener Lumineszenzmethoden zur Datierung von Löß. 23,--€
421. S., 56 Abb., 20 Tab.
422. WEBER, J. (2000): Kieselsäurediagenese und gekoppelte Sedimentarchitektur -eine Beckenanalyse 43,--€ des Reinhardswald-Troges (Norddeutsches Becken, Solling-Folge, Mittlerer Buntsandstein).
423. S., 107 Abb., 14 Tab., 11 Taf.
424. LAMPE, C. (2001): The effects of hydrothermal fluid flow on the temperature history of the northern 28,--€ Upper Rhinegraben: Numerical simulation studies. 126 S., 63 Abb., 5 Tab.
425. MINWEGEN, E. (2001): Die Biokonstruktionen im Pennsylvanium des Kantabrischen Gebirges 30,--€ (Nordspanien).
426. S., 61 Abb., 18 Taf.
427. ARETZ, M. (2002): Habitatanalyse und Riffbildungspotential kolonialer rugoser Korallen im 30.--€ Unterkarbon (Mississippium) von Westeuropa. 155 S., 57 Abb., 14 Taf.
428. NOÉ, S. (2003): Spätstadium einer sterbenden Karbonatplattform: Schelfrand-und Außen- 45.--€ schelfentwicklung der Tansill-Formation (Permian Reef Complex, New Mexico, USA).
429. S., 33 Abb., 38 Taf.
430. HIRSCHFELD, M. (2003): Isotopen-und Hydrochemie des Rheinsystems: Saisonale Variationen als 20.--€ Konsequenz dynamischer Prozessabläufe des kontinentalen Kohlenstoff-und Wasserkreislaufes.
431. S., 55 Abb., 5 Tab.
432. FREITAG, H. (2003): Proxydaten zur Bestimmung der meteorologisch-hydrologisch gesteuerten 23.--€ Variabilitäten des alpinen und nicht-alpinen Abflusses im Rheineinzugsgebiet während der letzten 150 Jahre. 108 S. 66 Abb., 1 Taf.
433. KEMNA, H.A. (2005): Pliocene and Lower Pleistocene stratigraphy in the Lower Rhine Embayment, 28.--€ Germany. 121 S., 35 Abb., 6 Taf.
434. ARETZ, M. & HERBIG, H.-G. (Eds., 2006): Carboniferous Conference Cologne. From Platform to 25. --€ Basin, September 4-10, 2006. Program and Abstracts. V + 130 S ARETZ, M. & HERBIG, H.-G. (Eds., 2007): Carboniferous Conference Cologne. From Platform noch nicht to Basin, September 4-10, 2006. Field trips -Carboniferous of the eastern Ardennes and the erschienen Rheinische Schiefergebirge GEREKE, M. (2007): Die oberdevonische Kellwasser-Krise in der Beckenfazies von Rheno- 35. --€ hercynikum und Saxothuringikum (spätes Frasnium/frühestes Famennium, Deutschland).
435. S., 49 Abb., 27 Taf.
436. ZACKE, A. (2007): Zahn-Apatit fossiler Selachier: ein Archiv zur Rekonstruktion von Paläökologie 25,--€ und Paläozeanographie warmzeitlicher Schelfmeere (Oberkreide-Paläogen, NW-Europa).
437. S., 51 Abb.
438. ARETZ, M. DELCULÉE, S. DENAYER, J. & POTY, E. (Eds., 2011): 11th Symposium on Fossil Cnidaria and Porifera, Liège, August 22-26, 2011, Abstracts, 202 S. ARETZ, M. & POTY, E. (Eds., 2011): 11th Symposium on Fossil Cnidaria and Porifera, Liège, August 22-26, 2011, Field Guides, 201 S.