Microfacies

The Vaca Muerta Formation in the Cerro Domuyo area shows an interesting intercalation of facies with opposite paleocurrents. The unit is represented by outer ramp to basinal facies with a westward direction of progradation. However, in its middle section, slope deposits correlatable with the Huncal Member, intercalate with slumped strata verging northeast. This interval is composed of carbonate facies and it is probably associated with the development of a slope related to a carbonate platform or a distally steepened carbonate ramp. Based on the ammonoid fauna, the age of the Vaca Muerta Formation ranges from the early Tithonian to the late Berriasian, but it could also reach the early Valanginian. The Huncal Member yields representatives of the Substeueroceras koeneni Biozone (Upper Tithonian), hence its age is older than that proposed in its type locality allowing its correlation with units exposed in the Chilean territory.

May, A. (1995b): Verwitterungsbeständigkeit und Verwitterung von Kalkstein-Naturbausteinen. - Münstersche Forschungen zur Geologie und Paläontologie, 77: 229-243, 6 figs., 2 tabs.; Münster.

Abstract: Weathering durability and weathering process of natural building stones from the Lower Muschelkalk, the Upper Muschelkalk, and the Devonian have been investigated. Various properties of each building stone and its limestone material are measured (microscopy, SEM, porosity, ultrasonic velocity, geochemical methods). Defined microfacies types show clear differences in their weathering durability. The quantities of the cold water absorption, the Schurecht ratio (= ratio cold/boiling water absorption), and the residue insoluble by hydrocloric acid strongly affect the weathering durability. Together with the investigation of thin-sections, these properties enable prognoses about the weathering durability. The limestones are mainly damaged by fissures which harm the unity of the stone. Probably these fissures are mainly based on frost phenomena. Connections between the sedimentary environment and the weathering durability are recognizable: generally limestones of the agitated (shallow) marine are more durable than other limestones.

Kurzfassung: Es wird die Verwitterungsbeständigkeit und Verwitterung von Naturbausteinen aus dem Unteren und Oberen Muschelkalk sowie dem Devon untersucht. Definierte Mikrofaziestypen zeigen deutliche Unterschiede in der Verwitterungsbeständigkeit. Die Größe der freiwilligen Wasseraufnahme, der Schurecht-Ratio und des Gehalts an salzsäureunlöslichem Rückstand beeinflussen die Verwitterungsbeständigkeit dieser Kalksteine stark. Der hauptsächliche Schaden an den Kalksteinen sind Risse, die wahrscheinlich durch Frostverwitterung entstehen. Es lassen sich Zusammenhänge zwischen dem sedimentären Environment und der Verwitterungsbeständigkeit erkennen.

The Asmari Formation, a thick carbonate succession of the Oligo-Miocene in Zagros Mountains (southwest Iran), has been studied to determine its microfacies, paleoenvironments and sedimentary sequences. Detailed petrographic analysis of the deposits led to the recognition of 10 microfacies types. In addition, five major deposi-tional environments were identified in the Asmari Formation. These include tidal flat, shelf lagoon, shoal, slope and basin environmental settings and are interpreted as a car-bonate platform developed in an open shelf situation but without effective barriers separating the platform from the open ocean. The Asmari carbonate succession consists of four, thick shallowing-upward sequences (third-order cycles). No major hiatuses were recognized between these cycles. Therefore, the contacts are interpreted as SB2 sequence boundary types. The Pabdeh Formation, the deeper marine facies equivalent of the Asmari Limestone is interpreted to be deposited in an outer slope-basin environment. The microfacies of the Pabdeh Formation shows similarities to the Asmari Formation.

L’étude de deux coupes lithologiques à Djebel Aoud Sma (Monts des Ouled Ali, Bordure Sud du bassin du Bas Chélif) a permis d’étudier la série messinienne complète de ce secteur. Les diatomites du Djebel Aoud Sma ont été subdivisées lithologiquement en deux membres. Les résultats ichnologiques ont permis de les placer au sommet du premier membre diatomitique du bassin du Bas Chélif. Les calcaires sus-jacents ont été subdivisés également en unité pré-récifale et unité récifale. Ils ont été le siège d’apports détritiques périodiques, qui ont atteint leur maximum dans l’unité récifale. L’Halimeda-rich beds ; un faciès qui pourrait constituer un niveau index, connu dans toutes les plates-formes carbonatées messiniennes de la Méditerranée occidentale, a été mis en évidence aussi, où il a été découvert pour la première fois dans la plate-forme carbonatée de la bordure Sud du bassin du Bas Chélif (Tessala-Béni Chougrane). L’étude microfaciologique a permis d’interpréter le milieu de dépôt des deux unités carbonatées. L’unité pré-récifale correspond à une plate-forme carbonatée peu profonde, envasée et relativement calme, tandis que l’unité récifale s’est déposée dans un milieu peu profond également, relativement agité, présentant un talus (pente récifale). Aussi, les résultats de la géochimie ont permis d’étudier la composition en éléments majeurs de tous les faciès rencontrés dans les marnes grises, les diatomites et les calcaires. Les diatomites pures peuvent constituer un bon gisement à exploiter, et c’est ainsi pour les calcaires qui peuvent faire une bonne matière première pour la fabrication du ciment gris et blanc.

Aspek mikrofasies dan diagenesis batuan karbonat Anggota Batugamping Formasi Pamutuan telah dipelajari guna mengetahui mekanisme pengendapan batuan dan sejarah proses geologi paska pengendapan batuan. Sampel-sampel batugamping yang telah diambil secara sistematis berdasarkan pada runtunan stratirafi hasil pengukuran penampang stratigrafi rinci pada formasi batuan yang berumur Miosen Tengah tersebut dan telah dipakai untuk bahan pengujian petrografi di laboratorium. Analisis petrografi telah dilakukan terhadap empat belas sampel batugamping yang memperlihatkan bahwa jenisnya adalah wackestone, packstone, grainstone, floatstone, rudstone, dan framestone. Lingkungan pengendapan batuan karbonat Anggota Batugamping Formasi Pamutuan tersebut meliputi fasies landaian laut dalam, tepian cekungan, lerengan terumbu depan, dan terumbu organik di tepi paparan. Beragam proses diagenesis yang terjadi pasca pengendapan batuan yang meliputi : penyemenan, pemikritan, pemampatan, neomorfisme, dan pelarutan.

En este trabajo se presentan datos que aportan conocimientos adicionales a los ya registrados para este lapso de tiempo en el noreste de México.

Hace aproximadamente entre 90 y 100 millones de años, durante el periodo Cretácico, específicamente durante el Albiano-Turoniano un aumento en el nivel del mar propició las condiciones para el desarrollo de una gran plataforma carbonatada.

En este trabajo se presentan los resultados del análisis de microfacies de una sección estratigráfica representativa de este evento transgresivo.

Three Paleocene-Eocene (P-E) stratigraphic transect sections namely, from the north to south, Ain Maqfi, Farafra-Ain Dalla road, and El-Quess Abu Said in the northern Farafra Oasis, Western Desert (Egypt) are described and interpreted based upon field observations, microfacies analysis, chronostratigraphy and foraminiferal paleobathymetry, to detect the effect of the Syrian Arc Fold System (SAFS) on the lateral and vertical facies changes, various stratigraphic breaks and to reconstruct the depositional paleo-environments. Lithostratigraphically, the P-E successions are composed of the upper part of the Dakhla Formation, Tarawan Chalk and Esna Shale Formation. Vertical and lateral facies changes are noted between tectonic paleo-highs and paleo-lows in the Farafra Oasis. Eight microfacies types are recognized. The larger benthic and planktonic foraminiferal zones are here used to correlate the shallow and deeper facies. Two larger benthic (SBZ4 and SBZ6), six planktonic foraminiferal (P4-E4) and one calcareous nannofossil (NP9b) biozones are identified. The recorded basal Eocene Dababiya Quarry Member (DQM) within the Esna Shale Formation in the central Farafra Oasis is represented by units 4 and 5 of the DQM at its GSSP with a neritic facies types. Towards the northern part of the Farafra Oasis, the P-E interval occurs within the base of the Maqfi Limestone Member that contains the larger benthic foraminiferal SBZ6 Zone and is correlated with the DQM. A major sea-level fall near the upper part of P5 Zone, followed by a prominent sea-level rise with a minor hiatus across the P-E interval in the Farafra Oasis reflects the complex interplay between sea level changes and tectonic signatures. Two inferred paleoenvironments, namely inner neritic and mid-outer neritic shelf have been identified.

Two Miocene sections in Cairo-Suez district at Tall Zamzam and Wadi Hommath are detailed examined for their foraminiferal, nannofossil contents and microfacies types. Wadi Hommath section is named as the Sadat Formation, while Tall Zamzam section is named as the Genefe Formation. 21species of planktonic, 20 species of benthic, 19 species of nannofossils are identified. Two zones of planktonic foraminifera and one zone of nannofossil attributed the Sadat Formation to Globigerinoides bisphericus (M4) Zone, Praeorbulina sicana (M5a) Zone and Genefe Formation to Praeorbulina glomerosa (M5b) Zone, while Helicosphaera ampliamperta Zone (NN4) of (Burdigalian-Langhian) age is recorded in the two studied secions. The identified benthic foraminifera was used to recognize three biofacies types: Nonion biofacies of inner-shelf environment, Cibicides biofacies of middle-shelf environment and Uvigerina biofacies of outer-shelf environment. Six microfacies types are identified. These successions are subdivided into three depositonal sequences of which 2 fourth order and one third order sequences.

Despite many advances in sea-level research, the nature of cyclic eustatic sea-level fluctuations during warm periods without, or with much reduced, polar ice remains enigmatic. Recently published δ18O records from extremely well-preserved Turonian microfossils from Tanzania do not support the contentious idea of glacioeustatic control of global sea-level changes during the warmest period of the Cretaceous. For the same locality (site TDP 31) we reconstruct relative sea-level changes based on sequence stratigraphy and integration of sedimentology, microfacies, geochemistry, and micropaleontology. Four local sequence boundaries (SBs TuTz1–4) are recognized: at the base, middle, and top of the Helvetoglobotruncana helvetica Zone and in the Late Turonian.
The lowstands are characterized by increased grain size, enhanced organic carbon flux, faunal assemblage changes, and bulk δ13Corg and foraminiferal δ13Cf and δ18Of minima. Strong benthic and planktic foraminiferal turnovers above the top Middle Turonian SB TuTz3 probably reflect shallowing (from upper slope to outer shelf) and/or eutrophication.
The TDP 31 age model is refined through inter-regional comparison of planktic foraminiferal ranges and δ13C records from three other South-Tethyan localities (ODP Holes 762C and 763B, Exmouth Plateau, and the Guru section, Tibet). This age model enables correlation of the regressive events at a global scale and suggests that, within stratigraphic uncertainty, the TDP 31 depositional sequences are synchronous with the global Turonian third-order sequences and are likely driven by eustasy. These correlations, together with recent astrochronological and radiometric dating, indicate a considerably younger age (91.17 ± 0.52 Ma) for the top H. helvetica Zone than currently assumed, resulting in zonal duration of 2.35 ± 0.52 myr. Foraminiferal stableisotope data fromTDP 31 indicate slight surface- and bottom-waterwarming during the regressions and possibly a minor surface-water salinity decrease,which is inconsistentwith glacio-eustatic forcing of Turonian third-order sea-level cycles and is more in line with the model of aquifer-eustasy.

In the Eifel area (western Rheinisches Schiefergebirge), a shallow-to deep-subtidal sequence of mixed carbonates and siltstones around the Kačák Event Interval close to the Eifelian-Givetian stage boundary was studied. An overall transgressive trend is inferred by the microfacies evolution. The stratigraphic variations of magnetic susceptibility in carbonates and in shale intervals show an overall decreasing evolution towards the top, which fits well with the transgressive trend. In addition, carbon and oxygen isotopes, and major, trace and rare earth element (REE) analysis have been used to get a better understanding of palaeoenvironmental variations in a shallow-water realm in the late Eifelian (kockelianus and ensensis conodont biozones): for example, the d 13 C excursion and Ce anomaly are interpreted to be the local representation of the beginning of the Kačák Event Interval, which is also consistent with the stratigraphy and microfacies analyses.

Abstract:  A moderately diverse larger foraminiferal fauna from the north-east Italian ‘Arenarie e calcari di S. Urbano’ formation with important stratigraphic, palaeoecological and palaeobiogeographical implications is described with respect to its position in the Western Tethys area. The fauna is dominated by hyaline perforated and porcellaneous forms including Amphistegina, Archaias, Austrotrillina, Miogypsinoides, Neoplanorbulinella, Neorotalia, Nummulites, Operculina and Spiroclypeus. The presence of Miogypsinoides complanatus allows the age of the formation to be determined as late Chattian (Shallow Benthic Zone SBZ 23). The palaeoenvironmental setting is interpreted as a shallow ramp environment ranging from (1) well lit, highly translucent, shallowest part of the photic zone characterized by Archaias and Austrotrillina, the deeper part of the inner ramp with Nummulites, to (2) the shallow part of the middle ramp with Spiroclypeus and miogypsinids and Operculina, to (3) a deeper middle-ramp setting dominated by coralline rhodoliths along with lepidocylinids. The presence of Archaias hensoni Smout and Eames shows that members of much more diverse Middle Eastern associations of shallow-water larger porcellaneous foraminifera are also present in the north-western parts of the Western Tethys, and reveals a corresponding diversity gradient among larger foraminiferal faunas in the Western Tethys, which is related to a decrease in temperature.

May, A. (1988a): Fossilführung und Palökologie des lagunären Massenkalkes (Devon) im Sauerland (Rheinisches Schiefergebirge). - Paläontologische Zeitschrift, 62 (3-4): 175-192, 6 figs., 4 tabs.; Stuttgart.

Abstract: The Massenkalk north of Brilon (East-Sauerland) and north of Balve (West-Sauerland) is of lagoonal character and is Upper Givetian (Middle Devonian) in age. Stromatoporoids, which can be subdivided into different growth forms (spherical to tabular, encrusting, thin laminar, branching), are the main reef building organisms. The species of the branching stromatoporoid Amphipora, which are hard to distinguish, dominate. The two thin laminar speciesStromatopora cygnea Stearn 1963 andStachyodes (Keega) jonelrayi Stearn 1975 are described for the first time from Western Europe. Tabulate corals represent about 20 % of the reef-builders and permit important inferences about the restriction of environment. Rugose corals and calcareous algae are rare. Reef dwelling organisms are less important, among these brachiopods, molluscs, foraminifera, calcispheres, and ostracods are, however, widespread. - Several associations of reef-builders that depend on different water depths can be distinguished. Their composition varies according to the restriction of environment. With increasing water depth water energy increased on the carbonate platform. The analysis of the stratigraphical distribution of the species of the reef-builder fauna allows no more but vague stratigraphical classifications.

Kurzfassung:  In den untersuchten Vorkommen nördlich Brilon (Ost-Sauerland) und nördlich Balve (West-Sauerland) besitzt der Massenkalk lagunären Charakter und gehört dem Ober-Givetium (Mittel-Devon) an. Die wichtigsten Riffbildner sind die Stromatoporen, die sich in verschiedene Wuchsform-Typen untergliedern lassen (kugelig bis tabular, inkrustierend, dünnlagig, ästig). Die beiden dünn-lagigen ArtenStromatopora cygnea Stearn 1963 undStachyodes (Keega) jonelrayi Stearn 1975 werden erstmalig aus Westeuropa beschrieben. Tabulate Korallen haben einen Anteil von ca. 20 % an der Riffbildner-Fauna. Rugose Korallen und Kalkalgen sind selten. Die Riffbewohner sind weniger bedeutend, unter ihnen sind Brachiopoden, Mollusken, Foraminiferen, Calcisphaeren und Ostracoden am wichtigsten. -Es lassen sich mehrere Riffbildner-Vergesellschaftungen unterscheiden, die für verschiedene Wassertiefen charakteristisch sind. Ihre Zusammensetzung wird von der Eingeschränktheit des Milieus beeinflußt. Die Riffbildner geben Hinweise auf die biostratigraphische Einstufung.

May, A. (1994d): Sedimentologie und Verwitterungsbeständigkeit des Wellenkalks (Unterer Muschelkalk) von Osnabrück. - Osnabrücker naturwissenschaftliche Mitteilungen, 19: 35-56, 10 figs.; Osnabrück.

Abstract: Sedimentology and weathering durability of the Osnabrück Wellenkalk limestone (Lower Muschelkalk) are investigated at stones from two building walls in Osnabrück and at sampies from the quarry of the Botanical Garden Osnabrück. Six microfacies types (A-F) are distinguished and described in detail. The microfacies analysis gives detailed informations about the sedimentary environment. Based on these informations the observed sedimentary cycles are attributed to sea-Ievel changes. The dinstinguished microfacies types show clear differences in their weathering durability. The best durability have the microfacies types A and B, which are tempestite layers in the lower and the upper part of the Oolith bank Member of the Wellenkalk Formation. The microfacies types A and B have such a good weathering durability, because they are not laminated and their quantities of the cold water absorption, the Schurecht ratio (= ratio cold/boiling water absorption), and the residue insoluble by hydrocloric acid are relatively low. 

Kurzfassung: Die Sedimentologie und Verwitterungsbeständigkeit des Osnabrücker Weilenkalks (Unterer Muschelkalk) werden an Mauersteinen aus zwei Gebäuden in Osnabrück und an Proben aus dem Steinbruch im Botanischen Garten Osnabrück untersucht. Es lassen sich 6 Mikrofaziestypen (A-F) unterscheiden, die ausführlich beschrieben werden. Ihre Analyse erlaubt detaillierte Aussagen zum Sedimentationsraum und zur Entstehung. Darauf aufbauend werden die in der Schichtenfolge beobachtbaren Sedimentationszyklen auf Meeresspiegeländerungen zurückgeführt. Es lassen sich deutliche Unterschiede in der Verwitterungsbeständigkeit der verschiedenen Mikrofaziestypen erkennen. Am verwitterungsbeständigsten sind die Mikrofaziestypen A und B, durch Sturmfluten entstandene Lagen im unteren und oberen Teil des Oolithbank-Members der Wellenkalk-Formation. Die Mikrofaziestypen A und B sind so verwitterungsbeständig., da sie nicht feingeschichtet sind und freiwillige Wasseraufnahme, Schurecht-Ratio (= freiwillige Wasseraufnahme geteilt durch effektive Porosität) sowie der Gehalt an salzsäureunlöslichem Rückstand relativ gering sind.

"Storm deposits (tempestites) have been extensively studied in the sedimentary record, particularly those deposits with hummocky cross-stratification, knowing their bathymetric ranks, facies models and their hydrodynamic conditions (Harms et al., 1975; Dott y Burgeois, 1982; Dumas y Arnott, 2006). However, detailed studies in carbonate sediments are relatively scarce. Recently, other types of interference generated at the picnocline interface (internal waves) were proposed to interpret similar deposits without being controlled by the position of the of storm-wave level (Pomar et al., 2012). The Tithonian - Valanginian deposits in the southern Mendoza - Neuquén Basin are particularly interesting because of their association with a homoclinal carbonate ramp system. During the Late Jurassic - Early Cretaceous a series of marine sequences were developed throughout the basin that are grouped under the Mendoza Group. In the southern Mendoza area it includes the Vaca Muerta Formation (early Tithonian - early Valanginian), the Chachao Formation (early Valanginian) and the Agrio Formation (early Valanginian - early Barremian) (Figs. 1 and 2).
The Vaca Muerta Formation is widely distributed over the entire Neuquén Basin. It consists of dark bituminous shales, marls and limestones deposited in response to a rapid and widespread marine transgression originated from the Pacific Ocean, as consequence of a tectonic phase of compressional relaxation (Legarreta and Uliana, 1991). While initial studies show significant variations in the proportions of different lithologies, sedimentological knowledge is still general, with the exception of contributions from the south of the basin (Spalletti et al., 2000, 2008; Scasso et al., 2002, 2005) and southern Mendoza area (Doyle et al., 2005; Kietzmann et al., 2008, 2011).
Storm deposits are well developed in the Vaca Muerta Formation. Based on tempestites characteristics and their associated beds four distinct deposits have been identified in the Bardas Blancas area (Fig. 3): (1) packstones with lowangle cross-stratification, (2) packstones/grainstones with large scale hummocky cross-stratification, (3) rudstones/grainstones with small scale hummocky cross-stratification, and (4) laminated wackestones/packstones with intralaminar normal gradation (Figs. 5 and 6). Packstones with low-angle cross-stratification can be interpreted as anisotropic hummocks deposits or low relief megaripples generated under combined flows during major storms in the middle ramp. A complete sequence of HCS consists of three divisions (Sa-Sc) associated with the storm event, and an upper unit (Sd) that represents the fairweather period between major storm events. Unit Sa starts with an erosion base and consists in low angle cross-stratified rudstones/grainstones. Unit Sb The unit begins with a second order surface and is composed by packstones and grainstones with hummocky cross-stratification. Unit Sc is represented by peloidal packstones with ripple marks, and finally the unit Sd consists of laminated wackestones/packstones. Laminated wackestones/packstones with intralaminar normal gradation consist of bioclastic wackestones/packstones composed of saccocomids remains or a rhythmic alternation of peloidal packstones and sandy layers with current ripple marks, which probably represents the distal expression of the storms. Variations from this sequence allow us to make some comparison with other ancient carbonate storm deposits (Kreisa, 1981; Monaco 1992, Sami y Descorchers, 1992; Molina et al., 1997; Zhou et al., 2011). Although deposits of the Vaca Muerta Formation are compositionally similar to those described by Molina et al. (1997), the ideal sequence is similar to that recognized by Monaco (1992) (Fig. 10). The division proposed by Monaco (1992) seems to be the most accurate, since it is based on the recognition of structures generated under different hydrodynamic conditions rather than genetic interpretations associated with the phases of the storm.
Comparing the described storm-influenced deposits with ancient and modern storm deposits examples, a relative water depth of 25 to 50 m is estimated for the formation of the HCS limestone facies. Even assuming its origin from internal waves, the position of the pycnocline in warm seas and small basins would be found within the same depth range (Nordberg et al., 2000), so that the deposits described in this paper may be important in future palaeogeographical studies in the Neuquén Basin."

Une description lithostratigraphique et une étude paléoenvironnementale des terrains messiniens affleurant sur la bordure méridionale du bassin du Bas Chélif en Algérie nord-occidentale sont présentées. L’étude est basée sur l’analyse de deux coupes levées au niveau des limites méridionale et septentrionale du Djebel Aoud Sma dans la région de Sig. Trois formations ont été identifiées et interprétées sur le plan environnemental : (i) les Marnes grises, attribuées au Messinien et déposées dans un milieu de vasières profondes ; (ii) les Diatomites, caractérisées par des bancs diatomitiques et des diatomites marneuses à caractères infra- à circalittoraux ; (iii) les Calcaires, correspondant à des calcaires récifaux et péri-récifaux, dans lesquels cinq faciès ont été individualisés.
Le faciès calcaire à Halimeda enregistré dans la coupe de Haoudh el Matmar a été mis en évidence dans le présent papier. Ce faciès, connu dans tous les bassins marginaux de la Méditerranée occidentale, évoque des changements environnementaux importants. Ainsi, il constitue un niveau index permettant la corrélation avec toutes les autres plates-formes carbonatées péri-méditerranéennes.

Lower Oligocene, shallow-water carbonates of the Calcareniti di Castelgomberto formation (Monti Berici, Italy, Southern Alps) are studied in detail with respect to fabric and component distributions in order to trace paleoecological changes along a monotonous sedimentary stacking pattern. The carbonates are dominated by coralline algal rudstones with a packstone to wackestone matrix. Non-geniculate coralline algae include six genera: Lithoporella melobesioides, Mesophyllum, Neogoniolithon, Spongites, Sporolithon, and Subterraniphyllum. The algae are found in the form of encrusting thalli, rhodoliths, and coralline debris. Non-algal components include larger, small benthic, and planktonic foraminifera associated with bryozoans, zooxanthellate corals, and echinoderms. Four carbonate facies are distinguished: (1) coralline algal facies, (2) coralline algal-coral facies, (3) coralline algallarger foraminiferal facies, and (4) coralline algal debris facies. Marly horizons also occur in the section. The facies and coralline algal content are interpreted with respect to light intensity, hydrodynamic energy, biotic interactions, and substrate stability. Facies development along the studied section shows systematic variations, suggesting asymmetric sea-level changes with rapid regressions and gradual transgressions.

The Faciès Rognacien is a sequence of highly bioturbated and pedogenically
modifi ed palustrine carbonates that were deposited under oxic conditions around the
Cretaceous-Tertiary (K-T) boundary in the northeastern Pyrenean foreland basin
(SW France). The sedimentary structures and early diagenetic features identifi ed
(mottling, nodule formation, brecciation, pseudomicrokarst, cracking, charophytes,
Microcodium) suggest deposition in a palustrine environment between the subarid
and intermediate climate type. Sedimentological and paleoecological analysis enables
us to distinguish two facies associations, the lacustrine pond facies and the freshwater
marsh facies associations. The majority of the carbonates are attributed to the
freshwater marsh facies. The lacustrine pond facies occurs only in isolated paleolows,
and is identifi ed on the basis of its paleobiological content (charophytes, ostracodes).
This suggests that the palustrine carbonates of the Faciès Rognacien were deposited
in a seasonal wetland (carbonate-producing freshwater marsh), rather than in the
marginal zone of a large, shallow lake. In this wetland paleoenvironment, all carbonates
underwent widespread pedogenesis, and small, ephemeral ponds are of limited
distribution, most likely recording deposition in paleolows.

Survey of Slovak Rcpuhlic. Mlynski dnlino I . SK-3 17 04 BratisTavn. Slovakia. c-marl: rakt~[email protected] '~niver.iit!:oTMit~ing and Mt.iallurgy. : .4ncE1~ci.Wier~ho\\~~lii(ifi11~1".rdu.pI ?I brflrr~.r. Ari a21;intluncd qu:irry at B e i i :~~i~i a Klil~pc in thc Picniny Kltppcn Belt ill c:lqtcm SlnvnLi:i shows the complete s~lvcession nt Lorvrl Jurawic to PJppcr Jurassic {Orfodinn I deposits zvcll clared by ammvnire ~:ILInnf. Thc Lnwer Juraxsic inclutleu: sandstonec, and sandy rnarlc (DRIIT~ Mlyn Fm,. :'Hrttangian -E,uIy Sintmurian). <potty limestnncs and rnklrrls (AIlgBu Fm.. Latc Siiicmurian -Latc Dotnerinn). glaucon~tic sondstnncs nad ~n~r l s r o n r .~ (Ilc*lrk:i Fm.ncw fnr~nnlion. Latc Dcrmer~;ln). red marls (Hfbnk Marl Fm.ncw formation. To:~rcinn). Tlic Mirldle J~~rns\ic p311 li>C the M I C C C I~~O R cnniprisc~ thick crritoidal limestone formation I Aalcni.m -Rn,jucinn I ri~forrnally 511 Wivitled into t1irc.c members: Mvfemher Aal ternnticm of marly crinr)id;~l lime<-to~lcs 2nd grey marls. Mclnher Rn'tldich critirjidal lirncqtones, p;lr~ly nr~dul:rr, with infclrnlations ol' rcd norlt~lar micritic Ti~ncrtorics anrl cherts. Mernlrr C -~s e c~~i s l i and gre! urinoidal limcslnnes \v~tli bl;~ub chcrts. Tflcsc depnsrls ilrc abruptly n\ rrlnin L i l o~~y a rn:~rkc.d ilrnmi+rini~ rurk~ct h! . prlagic arnmnni~icn-ms~n type linlehtnncs of thf Cztlsr~ryr~ Lirnestttnr I:m. (1.atc R;!jociai~ -OltfnrcEi:~ril. The limc51onea arc rlrvclnped a5 ti-Inrt~cnlous ~t~icrtlljvics o f tlic latest Rajrjcian t~ c;lr[y Ralh(rnf;111 age and ic>llo\vctl hg lie Glrrhrtl;,~rt~it~~r microfacies yielding :~mm.clni~eh or Ox h r d $:in :ye. Thc Lower Crelacetlu? part of the urclrrwjon cni-responds I (> thc Nrin:i Fni. 11 consists cjf v:lriotlc deplsith sr~ch as vrinoid:~l lirnestonrr. ?r!msedirncntiiry li lncrif)ne brecci:) and mar!? cnntaining ah~indiint org;~nr~de~rital m:itcriirl (~r thc Urgoni:ln shallow-w:uer cnrhonnte platform oripin. Tlr: aucce.;si(,n (IT ilir. Rcil:l!ina Kllpps dirfcrs I'mnr 1ypic:ll w c~~\ s i r l n s nf thc Pitniny Klippen Basin. It mny bc i~~t t r p~~~~d ~' i t l i~r :IS :I 1.ilrit1' (lf file U7(1ti7tyn Si~~cc'isio~i. :lntl llitrs lrlcatecl in rlic norrlicrn p:m oC the h3411. or 2\.~11 ;~b C L I C L '~~< %~(~ depohitrd nl solltl~ern malein of Ihc I'izniny Klippen B;~sin. Snmc :lmmnnitr.; of E~trly J~rrassrc enrly Mirkllr Snr;~\sic so Tnr ~loorl!. knclwll h ) m ilic Wcst C:~rl,:tlhianr arc tlc\crihzd in 11ic pal:~conrrrlogic:il ptii-1 of' the paper. Tl~c.;c ilivl tide rcprcwntnllycs of Lyh~ei.;~t irl:lc i A I r r r r~l~~~r~t~~~r~~.~ ). Arictitid:ic (Cbtnrrrt-c,rtrr\. Hildncznridnr (I-'rrc.kir'l!ft) and Kmphocc~ttidae (I.rrdr~.t~yrr~, Gr<r/~hnrrr~~.!. Ih.c~rilirr I. Kt,! ~r.nrrlr: Jurnssiu. Western Cnrp:~thinns. Pieniny KBippen Relt. Imiver Crctxeoils. nrnrnonirc.~ L~t c s t gcolo~icnl rcscarrh ill Eastern Sloukian part of thc Pieniny Klippen Rclt (PKBI broughr new nnd importonr inrnrmntinn on litho$tmti,nmphic v3ri;lhility. P;IIContolryy and hios~ratig~iphy of' ~h c Jurassic 3i1d E;~rly

In order to interpret the microfacies and depositional environment of the Mishan Formation, two stratigraphic sections were studied in the Khorgu and Khamir anticlines at the north and west of the Bandar Abbas southern Iran. The Khamir section in the Khamir anticline includes: medium-bedded to massive limestone, medium-bedded dolomitic limestone, medium-bedded marly limestone, chalk and green marl. The Mishan Formation in the Khorgu anticline includes: medium to thick-bedded limestone, medium-bedded marly limestone, calcareous marl, grey marl and green marl. Two different facies types (i.e., clastic and carbonate facies) have been recognized in this study. Also, detailed petrographic analysis of the carbonate facies led us to the recognition of 12 microfacies types grouped into three major depositional environments (inner, middle and outer shelf) in Khamir section and two depositional environments in Khorgu section (middle shelf and outer shelf). The inner shelf facies is characterized by mudstone, wackstone, packstone and grainstone,dominated with miliolid, Dendritina, bryozoa and small perforate foraminifera dominated microfaunas. The middle shelf facies is represented by wackstone to packestone with diverse assemblage of large perforate benthic foraminifers, Ditrupa and the rare planktonic foraminifers. Outer shelf facies is dominated by planktonic and perforate foraminifers and Ditrupa.

May, A. (1998c): Verwitterung und Verwitterungsbeständigkeit von Naturbausteinen aus Kalkstein am Beispiel des Osnabrücker Wellenkalks (Trias). - Neues Jahrbuch für Geologie und Paläontologie Abhandlungen, 208: 637-651, 6 figs.; Stuttgart.

Abstract: New results about the weathering decay and weathering resistance of limestone building stones are presented by the example of the Osnabrücker WeIlenkalk (Lower Muschelkalk), an important building stone in the vicinity of Osnabrück (Northern Germany). Weathering decay and weathering resistance of its varieties are investigated at stones from two building walls in Osnabrück. The limestones are mainly damaged by fissures essentially based on frost phenomena. The dimensions of the building stone influence its weathering decay. Remarkable differences of the weathering resistance are visible between the six distinguished varieties (microfacies types A-F). The mircofacies types A and B are best resistant against weathering, because they are not laminated, and the quantities of the cold water absorption, the Schurecht ratio (ratio cold/boiling water absorption), and the residue insoluble by hydrochloric acid are relatively low.

Zusammenfassung: Neue Forschungsergebnisse zur Verwitterung und Verwitterungsbeständigkeit von Mauersteinen aus Kalkstein werden am Beispiel des Osnabrücker Wellenkalks (Unterer Muschelkalk), einem wichtigen Naturbaustein, dargestellt. Die Verwitterung und Verwitterungsbeständigkeit seiner Varietäten werden an Mauersteinen aus zwei Gebäuden in Osnabrück untersucht. Die Mauersteine werden hauptsächlich durch (lang aushaltende) Risse geschädigt, die im wesentlichen auf Frost- Tau- Wechsel-Prozessen und Frostsprengung beruhen. Es lassen sich deutliche Unterschiede in der Verwitterungsbeständigkeit der sechs im Osnabrücker Wellenkalk unterschiedenen Gesteinsvarietäten (Mikrofaziestypen A-F) erkennen. Am verwitterungsbeständigsten sind die Mikrofaziestypen A und B, die geringmächtige Lagen bilden. Die Mik.rofaziestypen A und B sind so verwitterungsbeständig, da sie nicht feingeschichtet sind und freiwillige Wasseraufnahme, Schurecht-Ratio (= freiwillige Wasseraufnahme geteilt durch effektive Porosität) sowie der Gehalt an salzsäureunlöslichem Rückstand relativ gering sind.

"Subtropical carbonates from the Callovian Calabozo Formation, and their diagenesis, Neuquen Basin, MendozaPprovince. Detailed study of Callovian carbonates of the Calabozo Formation (30 m) in western Argentina, reveals the abundance of benthic carbonates particles produced by organisms that are light dependent, and non-skeletal grains such as ooids and peloids. The biota consists of bivalves, dasyclads (Salpingoporella annulata Carozzi, Cylindroporella annulata Carozzi, and Heteroporella sp.), scleractinian corals, echinoderms, cyanobacteria (Cayeuxia (Rivularia) piae Rech-Frollo, and Cayeuxia (Rivularia) kurdistanensis Elliot), oncoids, gastropods, forams, and calcispheres as well as ostracods, and bryozoans in relatively minor quantities. Allochemical particles suggest for the shallow marine limestones of the Calabozo Formation a Photozoan
Association under subtropical seawater conditions. The petrographic features allow to recognize seven microfacies, differentiated by particle types, fossils and depositional texture: 1) criptalgal bindstone; 2) bioclastic-peloidal wackestone; 3) bioclastic-intraclastic wackestone; 4) bioclastic-peloidal-
terrigenous wackestone, 5) coral framestone, 6) peloidal-bioclastic-intraclastic packstone, and 7) oolitic-bioclastic-peloidal packstone-grainstone. The recognition of microfacies groups constitute two palaeoenvironmental associations: inner ramp and middle ramp settings. Diagenetic studies are based on examination of stained thin sections, through conventional petrography and under cathodoluminescence. Early diagenetic processes are micritization and precipitation of peloidal micrite and acicular calcite. These cements predate granular and syntaxial calcite cemets. Cathodoluminescent petrography allows to identify three morphologic types of clear cements: (1) fine acicular crystals, (2) granular cements, and (3) syntaxial cement rims on echinoderm particles. Description of the CL signature has evolved to discrimination as either, non-luminescent, dully luminescent red/orange, or brightly luminescent yellow. The earlier acicular calcite cement is non-luminescent, on the other hand, the predominantly
dully luminescent red/orange, or brightly luminescent yellow of interparticular and intraparticular granular calcite and syntaxial cements indicate a shallow burial meteoric-phreatic diagenetic environment."

May, A. (1997b): Mikrofazies und Zyklizität der Wellenkalk-Formation (Unterer Muschelkalk) von Osnabrück (Norddeutschland). - Zentralblatt für Geologie und Paläontologie Teil I, 1996 (5/6): 521-532, 1 figs., pl. 1; Stuttgart.

Abstract: The Wellenkalk Formation (Lower Muschelkalk) has been investigated at the Westerberg within Osnabrück (Northern Germany). The microfacies types A and B build thin tempestite layers. Within the "Wellenkalke" the microfacies types C to E can be distinguished by decreasing intensity of bioturbation. The microfacies type F represents the "Gelbkalke". In an ideal cycle the sequence of microfacies types is: A or B - C - D to E - F. The microfacies types A and B were sedimented between the storm wave base and the normal wave base. The microfacies type F originated in the high intertidal and supratidal zones. The microfacies types of the "Wellenkalke " are built within following zones: C = subtidal, D and E = shallow subtidal and intertidal.

Zusammenfassung: Die Wellenkalk-Formation (Unterer Muschelkalk) wurde am Westerberg in Osnabrück (Norddeutschland) untersucht. Die Mikrofaziestypen A und B bilden dünne Tempestit-Lagen. Innerhalb der Wellenkalke lassen sich mit abnehmender Bioturbation die Mikrofaziestypen C bis E unterscheiden. Mikrofaziestyp F repräsentiert die Gelbkalke. In einem Idealzyklus ist die Folge der Mikrofaziestypen: A oder B - C - D bis E - F. Die Mikrofaziestypen A und B wurden zwischen Sturm- und Schönwetter-Wellenbasis abgelagert, und der Mikrofaziestyp F entstand im hohen Intertidal und Supratidal. Die Wellenkalk-Mikrofaziestypen sind: C = Subtidal, D und E = flaches Subtidal und Intertidal.

Uppermost JUrassic? -NeocomiaN shallow-water carboNates of the blake Nose, Usa: DsDp site 392a revisiteD felix schlagintweit 1 & paul enos 2 abstract Upper Jurassic (?) to Valanginian shallow-water limestones were recovered at DSDP Sites 390 and 392, on the Blake Nose at the seaward edge of the Blake Plateau in 1975. Re-examination of the microfacies and the benthic foraminiferal and calcareous algal biota suggests a possible Late Jurassic age for the oldest limestones. The widely recognized intra-Valanginian unconformity extends to the northeastern margin of the Late Jurassic-Early Cretaceous carbonate megaplatform in the western Atlantic. keywords Microfacies, calcaraeous algae, Dasycladales, foraminifera, stratigraphy, USA fig. 2 -Lithostratigraphic log at Site 392A (modiied from Enos & Freeman, 1978: Fig. 2) with selected microfossils (benthic foraminifera, dasycladalean algae). Stars = single occurrences.

May, A. (1997a): Verwitterungsbeständigkeit und Verwitterung von Naturbausteinen aus Kalkstein. - Geologie und Paläontologie in Westfalen, vol. 48: p. 3-185, 94 figs., 2 tabs., pl. 1-11; Münster.

Abstract: Weathering durability and weathering process of natural building stones from the Lower Muschelkalk, the Upper Muschelkalk, and the Devonian have been investigated. Various properties of each building stone and its limestone material are measured (microscopy, SEM, porosity, ultrasonic velocity, geochemical methods). Defined microfacies types show clear differences in their weathering durability. The quantities of the cold water absorption, the Schurecht ratio (= ratio cold/boiling water absorption), and the residue insoluble by hydrocloric acid strongly affect the weathering durability. Together with the investigation of thin-sections, these properties enable prognoses about the weathering durability. A diagram of correlation between coldwater absorption and Schurecht ratio is developed, which is able to discriminate more durable and less durable limestones by a boundary line (Fig. 59-60).The limestones are mainly damaged by fissures which harm the unity of the stone. Probably these fissures are mainly based on frost phenomena. Connections between the sedimentary environment and the weathering durability are recognizable: generally limestones of the agitated (shallow) marine are more durable than other limestones.

Kurzfassung: Es wurden die Unterschiede in der Verwitterungsbeständigkeit zwischen verschiedenen Varietäten jeweils eines Kalksteins untersucht. Beprobt wurden Kalksteine des Muschelkalks im Raum Osnabrück-Bielefeld und des Devons im Sauerland in Bauwerken und Aufschlüssen. Eine neue Klassifikation des Verwitterungszustandes von Kalkstein-Mauersteinen wurde entwickelt. Die Oberflächenschäden auf der Außenseite sind nur ± gering und stellen bloß ein "kosmetisches" Problem dar. Die Stärke der Schädigung des inneren Zusammenhaltes des Mauersteins durch Risse ist viel wichtiger, da sie die Sicherheit und Stabilität des Bauwerks gefährdet. Die Untersuchung von Dünnschliffen ermöglichte es, insgesamt 17 Mikrofaziestypen zu definieren und erstmalig Unterschiede in der Verwitterungsbeständigkeit zwischen den verschiedenen Mikrofaziestypen eines Kalksteins zu erkennen. Kalksteine, die in ± turbulentem (und damit ± flachem) Meereswasser abgelagert wurden, sind tendenziell verwitterungsbeständiger als solche aus anderen Ablagerungsräumen. Mit der Auftriebsmethode wurden wichtige Porositätsparameter festgestellt. Freiwillige Wasseraufnahme und Schurecht-Ratio (= Quotient freiwillige Wasseraufnahme / effektive Porosität) beeinflussen die Verwitterungsbeständigkeit sehr stark, wenn ihre Größe zunimmt, nimmt die Verwitterungsbeständigkeit ab. Die Ultraschall-Untersuchungen zeigten, daß in Kalksteinen Spannungen viel weiter geleitet werden als in Sandsteinen und deshalb zu (lang aushaltenden) Rissen führen. Die rasterelektronenmikroskopische Untersuchung erlaubte Aussagen über einzelne Aspekte des Verwitterungsprozesses. Die im salzsäurelöslichen Gesteinsanteil gemessenen Element-Konzentrationen spielen keine Rolle für die Verwitterungsbeständigkeit der Kalksteine.  Die Verwitterungsbeständigkeit der bearbeiteten Kalksteine wird am stärksten von freiwilliger Wasseraufnahme und Schurecht-Ratio beeinflußt. Der Einfluß des Gehaltes an salzsäureunlöslichem Rückstand ist erheblich geringer. Darüber hinaus spielen auch die Merkmale Feinschichtung und Kristallgröße (Mikritl Sparit) eine gewisse Rolle. Die Entwicklung von Stylolithen hat nur nachrangige Bedeutung. Einen sehr großen praktischen Nutzen für Prognosen über die Verwitterungsbeständigkeit verspricht die erstmalig ermittelte Grenzlinie Schurecht-Ratio/freiwillige Wasseraufnahme, die unabhängig vom Probenkollektiv überdurchschnittlich und unterdurchschnittlich verwitterungsbeständige Kalkstein-Mauersteine mit ziemlich großer Schärfe voneinander trennt. Darauf aufbauend wurden leicht durchzuführende Verfahren zur Auswahl besonders verwitterungsbeständiger Kalksteine entwickelt. Im Gegensatz zur vorherrschenden Literaturmeinung werden Kalksteine im wesentlichen durch Risse geschädigt, die wahrscheinlich aufgrund von Frosterscheinungen (bzw. Frost-Tau-Wechsel-Prozessen) entstehen und hauptsächlich durch Frostsprengung vergrößert werden. Da die Schädigung der Gesteinsoberfläche ± gering ist, kann die chemische Verwitterung für Kalksteine nicht wichtig sein. Hierdurch unterscheiden sich Kalksteine in ihrem Verwitterungsverhalten sehr stark von Kalksandsteinen.

"Thecideid brachiopods are poorly known brachiopods of debated phylogenetic relationships which occur from the Late Triassic to the Recent. Although well known in encrusting communities of
Jurassic and Cretaceous cryptic habitats, they have received less attention in Cenozoic environments. Extensive thin section analysis of circumalpine Paleogene carbonates (Late Eocene of
Austria as well as the Early Oligocene of Slovenia, the Inntal Valley and Northern Italy) has revealed the presence of thecideid brachiopods allowing for the analysis of their taphonomy,
component relationships and facies distribution. The complex morphology of the valves enables these brachiopods to be readily identified in thin section, even if highly fragmented or encrusted.
Component analyses using semi-quantitative and quantitative methods reveal that these brachiopods are most commonly associated with corals and coralline algae. The brachiopods are often included within complex encrustation sequences. Their palaeoecology thus closely mirrors that of Recent and fossil thecideid species which are characteristics of cryptic habitats in tropical and warm temperate seas. The potential of these minute brachiopods as palaeoecological indicators has been underestimated especially considering their ease of recognition in thin section not only of complete valves, but also of highly fragmented material. "

A new concept, termed ‘Facies Dynamics’ (defined as changes of specific carbonate facies types in time and space, which are controlled by phylogenetic, ecological and geological parameters), is introduced. This concept aims to define and interpret spatial and temporal changes of carbonate facies patterns. It is based on Middle Eocene to Early Oligocene shallow-water carbonate facies types from the circumalpine area (north-eastern Italy, northern Slovenia, Austria and southern Bavaria), which are compared with respect to dominating biogenic components and their distributions along a shelf gradient. This comparison has lead to the distinction and definition of 14 Major Facies Types (MFTs), which are dominated by coralline algae, larger and smaller foraminifera, corals and bryozoans. The presence and distribution of these MFTs from three different time slices (Middle Eocene, Late Eocene and Early Oligocene) is compared. Nine aspects of facies dynamics are distinguished: origination, extinction, immigration, emigration, expansion, reduction, stasis, shift, and replacement of MFTs. These changes are controlled by regional changes in ecological parameters, but also by global events, especially extinction patterns at the Middle/Late Eocene boundary and at the Eocene/Oligocene boundary.

Carbonate mounds are widespread in many places around the world and are especially well exposed in the Cantabrian Mountains, northern Spain. This study focuses on the composition and growth dynamics of two large mound complexes well exposed near the village of Puebla de Lillo, 70 km northeast of León, and evaluates the impact of sea level, accommodation, and siliciclastic input on mound growth.

In the easternmost part of the Izeh Zone of the Zagros Mountains, the Kazhdumi Formation of upper Aptian-middle Albian interval is superbly exposed in three-main exposures as argillaceous carbonate facies. The main bioclastic components of the Kazhdumi Formation are Orbitolinid and other larger benthic foraminifers, planktonic foraminifera and calcareous algae. The depositional system in the study area during the upper Aptian-middle Albian corresponds to a shaly carbonate ramp. Two depositional sequences are determined, as prograding system from west to east. Comparison of the proposed depositional sequences with those reported in the Arabian Plate and adjacent areas suggests a correlation with the global sea-level curve. The Lower Cretaceous, Aptian carbonates of Kazhdumi Formation contain nine microfacies, which were deposited on a ramp system deepened in both directions (west and east). Stratigraphic sequence led to recognize two third-order sequences. On the other hand, rudstone and boundstone lithofacies of the studied formation have higher reservoir potential and were deposited during Apt 3 and Apt 5 sequences of the Arabian Plate. The Kazhdumi Formation in the study area was deposited in an intrashelf basin that should be classified as an independent basin in the future paleogeographic maps of the southwest Iran. We interpret the Kazerun Fault, as a crustal warping of basement faults of the Arabian Plate boundary, which were responsible for the creation of the intrashelf basin in the study area.

May, A. (1994a): Microfacies controls on weathering of carbonate building stones: Devonian (northern Sauerland, Germany). - Facies, 30: 193-208, 1 figs., 2 tabs., pl. 37-39; Erlangen.

Summary:    The Beisinghausen Limestone (Upper Givetian to Frasnian) in the Eslohe-Reiste area (northern Sauerland), used in the past as building stone, corresponds to proximal carbonate turbidites which have been derived from the Attendom-Elspe ‘reef’ complex. The particles of this allodapic limestone originated in different parts of the carbonate complex as shown by facies-diagnostic microfossils (foraminifera, calcisphaeres, calcareous algae, microproblematica). The fossils as well as the other dominating grain types (lumps, peloids) point to source areas located within lagoonal and slope environments. Reef-derived material is rare.  The turbidites exhibit four microfacies types, differentiated by composition and size of the grains as well as by micrite content and corresponding to the common vertical and lateral textural variation of limestone turbidites.  These MF types were recognized in outcrops as well as from building stones used in building the St. Pankratius church in Eslohe-Reiste (northern Sauerland) in 1849 and in the renovation of the church in 1963/64.  The comparison of microfacies and the degree of the destruction of ‘old’ and ‘new” building stones by weathering (macroscopically described by the ◂Fabric Index’: Product of the ‘Rock Destruction Risk’ and the ‘Rock Preparation Destruction Degree’) shows that intrabioclastic rudstones (MF type 1) and bioclastic grainstones (MF type 2), both characterizing the basal parts of the turbidite beds, are more resistant to weathering destruction originating from freezing and thawing than packstones (MF type 4). Weathering of micritic facies types (e.g., MF 4) is more intensive due to the stronger development of joint systems affecting not only the surface of the building stones but the entire dimension stone.  Porosity or the existence and amount of stylolites seem to have had no significant impact on the weathering of the building stones studied. The stronger weathering of building stones used in the original construction of the church as compared with the stones applied in this century is caused by the greater time interval available for mechanical weathering connected with freezing and thawing.  The consideration of microfacies of limestone turbidites should facilitate the exploitation of weathering-resistant carbonate building stones.

In this study, stratigraphic section of Nammal Formation (Early Eocene) of the Western Salt Range exposed in the Nammal Gorge is measured, sampled and logged. The 76m thick section of Nammal Formation at Nammal Gorge consists of predominantly slope forming limestone with interbedded shale, recessive limy siltstone and marl. The recessive beds are generally exposed above and below the limestone beds. The upper part of the Nammal Formation is exposed in a very steep cliff of wavy to flat bedded lime mudstone to packstone sequence. Four microfacies have been identified on the basis of petrographic studies; as Wackestone to Packstone Microfacies (NMF-1) deposited in middle ramp settings, Planktic Foraminiferal Mudstone to Wackestone Microfacies (NMF-2) representing open marine conditions of outer ramp settings, Wackestone Microfacies (NMF-3) showing deeper water environment of the outer ramp and Packstone Microfacies (NMF-4) depicting high energy conditions towards inner ramp. The various allochemical constituents of the formation have been identified which include different varieties of foraminifers e.g. Benthic Foraminifera; Assilina dandotica, Assilina laminosa, Assilina leymerie, Assilina spinosa, Nummulites globulus Leymerie, Nummulites atacicus Leymerie, Nummulites mammalitus, Discocyclina dispansa, Discocyclina ranikotensis, Lockhartia conditi, Operculina, Bigenerina, Miliolids, Textularia and Planktic Foraminifera; Globigerina along with some echinoderms and algal fragments often embedded in sparry calcite or lime mud. The bioclasts outnumber all other grain types present. The occurrences of various key age diagnostic foraminiferal assemblages suggest maximum stratigraphic ranges through foraminiferal shallow benthic biozones (SBZ 8/9-11) of Ypresian time. On the basis of fossil assemblages and textural relationships, the environment of deposition is interpreted to occur dominantly in the middle to outer ramp and less dominant towards inner ramp settings of the carbonate platform.

The present study deals with the identification of larger benthic foraminifera, establishing microfacies and the digenetic analysis of Margalla Hill Limestone based on field and petrographic data from the Sajikot Waterfall Section, District Abbottabad, Pakistan. The Margalla Hill Limestone predominantly composed of nodular limestone along with subordinate marl and shale is about 172m thick at Sajikot Waterfall Section in Hazara Basin, Lesser Himalayan region of Pakistan. The strata are horizontal to nearly vertical in this section. The lower contact of this formation is observed with Patala Formation of Paleocene age while its upper contact is not exposed in our studied section. Important species of benthic foraminiferal assemblages identified in this formation after a detailed petrographic study are Nummulites atacicus, Nummulites mamillatus, Nummulites globulus, Lockhartia tipperi (Davies), Lockhartia conditi, Lockhartia conica, Lockhartia diversa, Assilina granulose (d'Archaic), Assilina subspinosa, Assilina laminose, Ranikohtalia sahni (Davies), Ranikothalia nuttalli (Davies, 1927), Ranikhothalia sindensis, Discocyclina ranikotensis, Discocyclina dispansa, Operculina patalensis, Kathina selveri , Idalina sinjarica, Setia tibetica, Orbitosiphon punjabensis, Laffittenia bibensis, and Laffittenia erki. Following Microfacies of Margalla Hill Limestone have been recognized after the detailed sedimentological and paleontological studies; Foraminiferal Mudstone Microfacies (SMHMF- I), Foraminiferal Mudstone to Wackstone Microfacies (SMHMF- II), Foraminiferal Wackstone Microfacies (SMHMF- III), Foraminiferal Wackstone to Packstone Microfacies (SMHMF-IV). Based on the microfacies assemblages, the Margalla Hill Limestone is interpreted to have been deposited in the foraminiferal shoal and inner ramp to the proximal outer ramp area of the Tethyan carbonate platform. The larger benthic foraminiferal assemblages suggest that this formation represent the biostratigraphic interval equivalent to the Shallow Benthic Zone (SBZ 8-11) of Serra-Kiel et al. (1998) representing Ypresian stage of Lower Eocene. Stage III of the carbonate platform of Scheibner et al. (2005) has also been established in the studied section. The diagenetic features observed in the Margalla Hill Limestone at the studied section are pressure dissolution (Stylolites), calcite-filled microfractures, multiple calcites veins, disorientation/ dislocation of the bioclasts, micritization, neomorphism and fossils dissolution.

The present study is focused on the detailed investigation of benthic foraminiferal assemblages and interpretation of microfacies of the Lockhart Limestone in the field section located along Pail-Khushab Road, Central Salt Range, Pakistan. The formation is predominantly comprised of nodular limestone with occasional shale intercalations. Important species of Larger Benthic Foraminifera identified in the studied section of Lockhart Limestone include; Miscellanea miscella, Miscellanea juliettae, Lockhartia haimei, Lockhartia conica, Lockhartia conditi, Lockhartia tipperi, Ranikothalia sindensis, Ranikothalia sahni and Discocyclina ranikotensi along with Dasycladale algae and Miliolids. As per correlation with the Tethyan shallow benthic zonation scheme proposed by Serra-Kiel et al. (1998), the (SBZ 3-5) of Late Thanetian age is assigned to the section based on the age diagnostic species of foraminiferal assemblages. Restricted inner ramp to Proximal mid ramp settings of the Tethyan carbonate platform are represented by; Mudstone Microfacies (LFMF-1), Mud-Wackestone Microfacies (LFMF-2), Wackestone Microfacies (LFMF-3), Wacke-Packstone Microfacies (LFMF-4) and Packstone Microfacies (LFMF5) observed in the stratigraphic section. Different diagenetic features which are identified in Lockhart Limestone are; dolomitization, neomorphism, compaction, dissolution, micritization of bioclasts and fracture fillings.

In this paper, to study biostratigraphy of Paleogene deposits based on foraminifera fauna in NW of Jiroft located in the Central Iran
zone, two stratigraphic sections, namely Sabzevaran (354 m) and Sad (132 m) sections were selected. Planktonic foraminifera and
large benthic foraminifera were identified in both sections. Faunal assemblages and vertical distribution of identified species support
presence of 5 planktonic foraminiferal and 2 large benthic foraminiferal biozones in the Sabzevaran section showing Middle Eocene to
Chattian age. In addition, presence of planktonic foraminiferal assemblage along with 2 large benthic foraminiferal biozones confirms
the Late Eocene to Chattian age for the Sad section.

The Pieniny Klippen Belt is a tectonic melange representing the boundary between the Outer and Central Western Carpathians. Within this melange, Jurassic and Cretaceous sedimentary rocks from deep-water (Kysuca Basin) to shallow-water environments (Czorsztyn Unit) occur. The Nižná Unit of the Pieniny Klippen Belt was distinguished as a particular development of the Kysuca Unit. As a result of a sea-level fall in the Barremian, the Barremian-Aptian Nižná Limestone Formation (organodetritic Urgonian-like facies) rests unconformably on older formations. At the base of this transgressional contact the newly discovered Tvrdošín Breccia Member occurs. This breccia consists of clasts of radiolarites, red limestones, white Calpionella limestones, and black chert nodules extracted from these limestones. The presence of breccia shows that the pre-Barremian strata in the Nižná Unit were eroded to relatively deep levels. This event was coeval with, and probably related to, the hiatus in other units situated on the Czorsztyn Swell. The Nižná Limestone Formation is overlain by the uppermost Aptian to Cenomanian pelagic marlstones, limestones and radiolarites at least 10 m thick. These are followed by flysch with exotic pebble material. Its age is younger than Cenomanian, which contradicts previous opinions. An earlier (Albian) onset of exotic flysches would be indicative of more southern units, close to the exotic Andrusov Ridge. This implies that the Nižná Unit was situated at the northern margin of the sedimentary area of the Kysuca Unit, closer to the Czorsztyn Swell, where the exotic flysch sedimentation came later.

Pohler, S.M.L., & May, A., & Schönlaub, H.-P. (2007): Pragian-Emsian Crinoidal Sand Banks and Stromatoporoid-Hydrozoan Buildups, Carnic Alps, Austria. - In: Vennin, E., & Aretz, M., & Boulvain, F. & Munnecke, A. (eds.):  Facies from Palaeozoic reefs and bioaccumulations,Mémoires du Musée d´histoire  Naturelle de Paris, 198: 175-177, 2-9 figs.; Paris.

LOCALITY. — Pragian/Emsian subtropical shelf edge, Carnic Alps Platform, adjacent to northern margin of Gondwana  (Schönlaub 1992).  STRATIGRAPHY. — Hohe Warte Limestone is a formation of the southern shallow water facies preserved in the  Kellerwand Nappe of the Central Carnic Alps (Kreutzer 1990, 1992a, b). Hohe Warte Limestone is 350 m thick and  preceded by Lochkovian crinoid limestone (neritic Rauchkofel Limestone) and succeeded by Seewarte Limestone (early  Emsian?), a lagoonal facies with Hercynella (Fig. 2). Crinoidal sand mounds occur in the lower part of the section and  are characterized by coarse carbonate sand with partially preserved crinoids surrounded by finer-grained crinoidal sand.  Stromatoporoid-hydrozoan buildups occur in the upper part of the section and form patchily distributed bioherms  of unknown thickness and extent surrounded by crinoidal debris (Bandel 1969).  FACIES AND MICROFACIES (Figs 2-9). — Above a crinoidal sand substrate (neritic Rauchkofel Limestone), the first  crinoidal bank facies progrades basinward in the Late Lochkovian to Early Pragian. Facies consists of crinoidal rudstone  with spar-filled open space structures and large crossections of crinoid calyces (Fig. 3). The amount of early marine  cements lining open space structures suggests that a framework existed which provided attachment sites for crinoids  (Figs 4, 5). Higher up in the section framestones with tabulate and rugose corals, stromatoporoids and hydrozoans  become abundant. They are accompanied by crinoidal grainstones with numerous calcareous algae. 

BIODIVERSITY AND TAPHONOMY. — Heritsch (1943) listed 4 species of crinoids which were found in boulders at the  base of Mount Seewarte: Cyathocrinus carnicus Charlesworth, Megistocrinus devonicus Charlesw., Melocrinus prostellaris  Frech, and Rhipidocrinus praecursor Frech. The large cross-section (Fig. 3) maybe Pernerocrinus, a common Lower  Devonian crinoid that also occurs in the Pragian Koneprusy reefs (J. Dzik, written comm., 2005). The floating bulbs  (loboliths) are very common in Silurian/Lochkovian boundary interval beds in the deeper water successions. The  good preservation of the crinoids indicates that they were deposited close to their area of origin. Crinoids produced  the large amounts of carbonate sand encountered in the lower Hohe Warte Limestone.  Stromatoporoids, tabulate and rugose corals and hydrozoans are the dominant reef builders in the upper Hohe  Warte Limestone. Plectostroma latens (Počta) (Fig. 6) is the most common stromatoporoid in the Hohe Warte together  with Actinostroma? Ex gr. clathratum Nicholson, both were previously described from Koneprusy (May 2002).  Schistodictyon? sp. is also present. The problematic hydrozoan Fistulella undosa Shuysky is very common and acts as  binder and encruster in the reef community (Figs 7, 8). Among the tabulate corals the ramose Scoliopora (Protoscoliopora)  puberulus (Janet) represents a baffling reef dweller (Fig. 4). Heliolitids are present with Heliolites aff. werneri Oekentorp  & Brühl, and Helioplasma aff. aliena Galle and favositids are represented by Favosites styriacus Penecke. All three form  small bulbous colonies. Two small encrusting species occur: Platyaxum (Roseoporella) altechedatense (Dubatolov) and  Aulopora (Mastopora) sp. They are accompanied by a small ramose form Coenites falsus Dubatolov. Two significant  species of rugose corals were identified, Stauromatidium aff. marylandicum (Swartz) and Fasciphyllum sp. Important  accessory reef biota are algae (Fig. 9), brachiopods, trilobites, gastropods and bivalves. 

DISCUSSION. — The crinoidal sand banks probably formed at a site of the shelf or ramp where shallowing resulted  in accumulation of sand bars that became quickly lithified. Storm events caused rip-up of partially lithified sandaggregates  that was piled up as rubble banks (much like present day ‘motus’) with large open space structures.  Subsequent cementation resulted in formation of elevated structures that provided holdfasts for crinoids and other  marine organisms (brachiopods, algae). The crinoid facies becomes progressively enriched with stromatoporoids and  corals, which probably formed patch reefs on a well-aerated high-energy subtidal shelf. The large amount of calcareous  algae seen in the thin sections are in contrast to the Koneprusy Limestone (CZ), which is time-equivalent to the Hohe  Warte Limestone but more reefal in character.

May, A. (1994i): Foraminiferen, Kalkalgen und andere Mikrofossilien aus dem Givetium und Frasnium (Devon) des Sauerlandes (Rheinisches Schiefergebirge). - Dortmunder Beiträge zur Landeskunde, Naturwissenschaftliche Mitteilungen, 28: 7-31, 19 figs., 2 tabs.; Dortmund.

Abstract: The Beisinghausen Limestone (Upper Givetian to Frasnian) from Eslohe-Reiste in the eastern Sauerland (Rhenish Massif) consists of proximal turbidites. The particles came from the Middle to Upper Devonian Massenkalk reef complex of Attendorn and Elspe and they can be attached to different parts of the reef complex. The Beisinghausen Limestone shows a remarkable rich content of microfossils, consisting of foraminifera, calcisphaeres, calcareous algae, and microproblematica. These microfossils are described. The content of microfossils of the Beisinghausen Limestone is compared with the content of microfossils of two Lower Givetian coral-limestone horizons from the northwestern Sauerland as weil as the content of microfossils of the Upper Givetian lagoonal Massenkalk from the Brilon reef complex in the eastern Sauerland (table 1-2).

Kurzfassung: Der Beisinghäuser Kalk (Ober-Givetium bis Frasnium) von Eslohe-Reiste im östlichen Sauerland besteht aus proximalen Turbiditen. Die Partikel stammen aus dem mittel- bis oberdevonischen Massenkalk-Riffkomplex von Attendorn und Elspe und lassen sich verschiedenen Bereichen des Riffkomplexes zuordnen. Der Beisinghäuser Kalk zeigt eine auffällig reiche Mikrofossilführung aus Foraminiferen, Calcisphaeren, Kalkalgen und Mikroproblematika. Die Mikrofossilführung des Beisinghäuser Kalkes wird beschrieben und sowohl mit der Mikrofossilführung von zwei Korallenkalk-Horizonten aus dem Unter- Givetium des nordwestlichen Sauerlandes als auch mit der Mikrofossilführung des obergivetischen lagunären Massenkalkes im Briloner Riffkomplex (Ost-Sauerland) verglichen (Tabelle 1-2).

PRAGIAN-EMSIAN CRINOIDAL SAND BANKS AND STROMATOPOROID-HYDROZOAN BUILDUPS, CARNIC ALPS, AUSTRIA LOCALITY. — Pragian/Emsian subtropical shelf edge, Carnic Alps Platform, adjacent to northern margin of Gondwana (Schönlaub 1992). STRATIGRAPHY. — Hohe Warte Limestone is a formation of the southern shallow water facies preserved in the Kellerwand Nappe of the Central Carnic Alps (Kreutzer 1990, 1992a, b). Hohe Warte Limestone is 350 m thick and preceded by Lochkovian crinoid limestone (neritic Rauchkofel Limestone) and succeeded by Seewarte Limestone (early Emsian?), a lagoonal facies with Hercynella (Fig. 2). Crinoidal sand mounds occur in the lower part of the section and are characterized by coarse carbonate sand with partially preserved crinoids surrounded by finer-grained crinoidal sand. Stromatoporoid-hydrozoan buildups occur in the upper part of the section and form patchily distributed bioherms of unknown thickness and extent surrounded by crinoidal debris (Bandel 1969). FACIES A...

The Oligocene shallow-water carbonates of the Lower Inn Valley (Tyrol, Northern Calcareous Alps) contain a rich coralline algal flora. These carbonates are known from two distinct settings: (1) autochthonous limestones and (2) debris flows intercalated with deeper water marls. The carbonate facies are dominated not only by crustose coralline algae (Corallinaceae, Rhodophyta), but also by smaller and larger benthic foraminifers, bryozoans, corals as well as lithoclasts of Triassic origin. Five species of coralline algae are identified and described in detail: Lithoporella melobesioides, Lithothamnion sp. A, Lithothamnion sp. B, Mesophyllum sp., and Sporolithon sp. The distribution of algal taxa shows distinct relationships to non-algal biota and substrates: L. melobesioides preferably encrusts other coralline algae, Lithothamnion sp. A is found encrusting bryozoans, Lithothamnion sp. B encrusts corals, while Mesophyllum sp. grows directly on fine-grained, soft substrates. Besides the fact that algal taxa reveal close relationships to other components, it can also be shown that algal assemblages are highly correlated to carbonate facies types. Hierarchical cluster analysis based on the relative abundance of taxa reveals five coralline algal assemblages showing distinct distribution patterns among carbonate facies. While two of the assemblages are restricted to the debris flows, the other three were found in both debris flows and autochthonous occurrences. A correlation between algal assemblages and carbonate facies allows the following conclusions to be made: (1) Both coralline algal taxa in particular and algal assemblages as a whole show distinct relations to water depth (herein referred to as a summary of light conditions and hydrodynamic energy) and substrate relationships. This makes them potentially valuable indicators for palaeoecological reconstructions. (2) Most of the coralline algal assemblages in allochthonous occurrences (i.e. debris flow) can be traced back to facies patterns in autochthonous occurrences. This indicates that a thorough microfacies analysis combined with a systematic study of specific components can be very useful in the reconstruction of palaeoenvironments, even if these are not preserved in their original context. (3) Some of the coralline algal assemblages within debris flows cannot be traced to autochthonous facies and do not seem to reflect primary facies compositions as they contain an atypical mixture of algal taxa and other components. These are characterised by a relatively high abundance of lithoclasts (usually >20% of the components) and a high degree of fragmentation of coralline algae thalli.

This article presents the conclusions reached in the authors PhD thesis called “Raw-material sources, raw-material supply and production strategies in the Upper Paleolithic from the Valachian Sector of Moesic Platform”. The study area is the Lower Danube Valley and it includes the Paleolithic sites of Vădastra-“Măgura Fetelor”, Ciuperceni-“La Tir”, Ciuperceni-“La Vii”, Giurgiu-“MaluRoşu” and Nicolae Bălcescu-“La Vii”, and a series of sampling points (see map 1, tables 1 and 2). The raw-material taken in consideration is chert. For many years archaeologist sustained two hypotheses about the raw-materials provenance: Pre-Balkan Platform and the Danube’s gravels. By means of macroscopic description in hand specimens, microscopic characterization in thin section (primary constituents, fossils) and X-ray Diffraction, the author has determined several varieties of chert for each site and sampling location and also three categories that present macro- and microscopic features that surpasses the local setting (see map 2, tables 4, 5 and 6). Taking count of microscopic features and by directly examining the thin sections of those varieties whit macroscopic similarities and from different places, the author determined the provenance of some raw-materials in the Paleolithic sites. The two Ciuperceni sites are linked to the Frăteşti Formation (Lower Pleistocene) gravels, opened in the vicinity by a modern quarry (Ciuperceni-“La Carieră”); some of the Giurgiu-“Malu Roşu” cherts were determined to come from gravels of the Frăteşti Formation, opened by modern quarries to the north (Ghizdaru-“Cariera de la Haltă”, Cetatea-“Cariera Bălănoaia”), and from gravels of the lower terrace (t1), opened in places such as Giurgiu-“Cariera Malu Roşu” and Giurgiu-“Cariera de la SV”; the source of provenance for the main raw-material (grayish “granulated” chert – in fact a peloidal chert) of Giurgiu-“Malu Roşu” was not found; for the other two sites in the study, Vădastra-“Măgura Fetelor” and Nicolae Bălcescu-“La Vii”, it hasn’t been possible to determine the provenance of the raw-materials. Al cherts form the Paleolithic sites present external characteristics similar to materials transported and reworked by waters (in spite of the “fresh cortex” present on many of the samples). Identified raw-material sources indicate short supply distances and a local exploitation of raw-materials.

This study is focused on the sedimentary environments, facies distribution and sequence stratigraphy of the Santonian intervals (Ilam Formation of Bangestan Group) that host enormous hydrocarbon reserves in five giant and supergiant oilfields in the central and southern parts of the Dezful Embayment (SW Iran). This reservoir formation is investigated using detailed petrographic analysis assisted by microscopic image analyses to explain its depositional facies and sedimentary environment in the subsurface sections of this embayment. Petrographic studies led to the recognition of 18 microfacies that formed in four facies belts: inner ramp (including shoal facies and open to restricted lagoons), mid-ramp (including channels and patch reef talus facies), outer ramp and basin. To locate the approximate position of the studied wells in the conceptual depositional model, frequency analyses for facies associations are carried out. The studied intervals consist of two, thick shallowing-upward 3rd-order sequences. Facies variations of the Ilam Formation investigated throughout the studied oilfields using correlation in a sequence stratigraphic framework.

The late Palaeozoic coal-bearing Madzaringwe Formation of the Karoo Supergroup in the Tshipise-Pafuri Basin in the Limpopo Province, South Africa, records part of the infill of a passive continental margin terrain. Lithofacies analysis was performed with a view to deduce the nature of depositional environments of the Formation. Sedimentological and sequence stratigraphic evidence indicates that this unit represents a complex siliciclastic facies that reflects a fluvial paleodepositional environment. Eleven facies, which were grouped into five facies associations, were recognised. The base of the Madzaringwe Formation (Lower Member) represents a sequence deposited by braided channels. The coal deposits represent flood plain and swamp deposits, which is characterised by shale, thick coal seams, siltstone, and sandstone. The Middle Member is characterised by both clast and matrix supported conglomerates, major tubular and lenticular sandstones, and finely calcareous, micaceous siltston...

The up to 258 m thick, carbonate-siliciclastic Upper Cenomanian to Campanian rocks (Sadr unit), which crop out widely in the Nakhlak area of central Iran, consist of conglomerates, sandy limestones and dolostones, calcareous sandstones, sandy-argillaceous limestones and reefal limestones. The lower boundary of the studied section is an angular unconformity and its upper boundary is faulted. Sedimentological and palaeontological data indicate that Upper Cretaceous Sadr unit of Nakhlak area is equivalent to shallow carbonate platform successions of Upper Cretaceous rocks in central Iran, which belong to the central Iranian Plate and were deposited in marginal marine, shallow shelf and moderately deep marine environments. This geological unit can be divided into carbonates, siliciclastics, and mixed carbonate-siliciclastics groups. The siliciclastic facies group was deposited as shorelines, tidal flats, lagoons, and barrier bars indicating shallow shelf environments. The mixed carbonate-siliciclastics facies group was formed in a coastal-delta complex and the carbonate facies group took initially place on a homoclinal ramp which later developed into a rimmed platform due to the expansion of the rudist barrier facies.

The up to 258 m thick, carbonate-siliciclastic Upper Cenomanian to Campanian rocks (Sadr unit), which crop out widely in the Nakhlak area of central Iran, consist of conglomerates, sandy limestones and dolostones, calcareous sandstones, sandy-argillaceous limestones and reefal limestones. The lower boundary of the studied section is an angular unconformity and its upper boundary is faulted. Sedimentological and palaeontological data indicate that Upper Cretaceous Sadr unit of Nakhlak area is equivalent to shallow carbonate platform successions of Upper Cretaceous rocks in central Iran, which belong to the central Iranian Plate and were deposited in marginal marine, shallow shelf and moderately deep marine environments. This geological unit can be divided into carbonates, siliciclastics, and mixed carbonate-siliciclastics groups. The siliciclastic facies group was deposited as shorelines, tidal flats, lagoons, and barrier bars indicating shallow shelf environments. The mixed carbonate-siliciclastics facies group was formed in a coastal-delta complex and the carbonate facies group took initially place on a homoclinal ramp which later developed into a rimmed platform due to the expansion of the rudist barrier facies.

In this study, the Eocene carbonate succession including Margalla Hill Limestone and Chorgali Formation representing the lower units of the Early Eocene Cherat Group have been investigated in the Margalla Hill Ranges and Hazara-Kashmir Basin. The field sections included, 1) Shahdara Section (Islamabad), 2) Khaira Gali Section (Galiat-Abbottabad) and 3) Yadgar Section (Muzaffarabad-Azad Jammu & Kashmir). Lithologically, these formations are comprised of predominant limestone units with occasional shale interbeds at places. Some notable fauna from the foraminiferal assemblage includes; Assilina spinosa, A. subspinosa, A. dandotica., A. granulosa, Lockhartia conditi, L. tipperi, Nummulites atacicus, N. globulus, N. mamillatus, Discocylina sp., Ranikothalia sp. etc. Presence of all these biostratigraphically significant shallow benthic foraminifera confirms that the deposition of Margalla Hill Limestone and Chorgali Formation occurred in Shallow Benthic Zones (SBZ 5/6 - SBZ12) of Ypresian time. The integrated depositional environment for Early Eocene Margalla Hill Limestone and Chorgali Formation from the studied sections is interpreted to occur between restricted inner ramp and distal mid ramp settings of carbonate platform. Restricted inner ramp, shoal, proximal mid ramp and distal mid ramp are important facies types represented by varying depositional textures of the studied carbonate succession. A very preliminary approach towards establishing stable isotopic stratigraphy at Paleocene/ Eocene boundary in one of the studied sections i.e. Yadgar Section is initiated. This study encounters a decrease in δ18O values along with pronounced decline in δ13C indicating quiet abrupt global extinction phenomenon at Paleocene/ Eocene Boundary.

In this study, two stratigraphic sections of Sarvak Formation were selected which are nominated Bavan and Kherameh sections. Over 379.5 meters of the Sarvak Formation and 260 thin sections have been studied. Index microfacies and foraminifers have been identified. Index microfacies include Boundstone, Wackestone and Packstone. The frequency of bioclast has been determined as larger that of the other microfacies elements. Based on the type and abundance of skeletal and nonskeletal grains and type of matrix, 14 sublithofacies have distinguished in 3 depositional environments which are include 1) Lagoon 2) Reef 3) Open marine. The mentioned determined microfacies were deposited in a Carbonate Platform of Homoclinal Ramp. Based on micropalentological data, the age of the Sarvak Formation is assigned to Cenomanian.