| Title Information | |
Lithostratigraphy and facies: The Cretaceous strata of the Pindos Zone can be subdivided into two basinwide formations, the Katafito Formation (Lower Cretaceous-Coniacian; two different facies) and the Platy Limestone Formation (Coniacian-Maastrichtian; four members). These formations comprise a mixed carbonate-siliceous-siliciclastic system with the fundamental depositional environments of deep basins: slope apron, submarine fan and basin plain. (Hemi-)pelagic sedimentation is represented by red claystones and radiolarites ("radiolarite facies" of the Katafito Formation) and pelagic biomicrites of the Platy Limestone Formation. Allochthonous deposition predominated the Upper Cretaceous development, occurring in four major phases of turbidite shedding (turbidite intervals). The lower two intervals resemble the "clastic facies" of the Katafito Formation in the lower Upper Cretaceous, the upper turbidite intervals constitute the carbonate mass-flow facies of the Platy Limestone Formation (slope apron of the higher Upper Cretaceous).
Lower Cretaceous to Lower Cenomanian: This period of time is represented by the radiolarite facies of the Katafito Formation (part one of this study). Emphasis has been given to the complex sedimentological and event-stratigraphic pattern as well as to the radiolarian fauna. Biostratigraphic age estimates of radiolarian assemblages were obtained by using and combining the most recently published range charts. This new data allows a precise litho-biostratigraphic description and interpretation of the thin, siliceous Lower Cretaceous interval.
The most apparent feature to be recognized and defined was the intercalation of five major green levels associated with organic-rich black shale layers. The Aptian-Albian green levels, especially the Lower Aptian one, can be interpreted as probable expressions of the mid-Cretaceous Oceanic Anoxic Events (OAE 1 and OAE 1a respectively). Further events occur in the Cenomanian-Coniacian radiolarite facies.
Furthermore, in the Barremian-Lower Aptian and the Upper Albian sections, petrographic and microfacies analysis revealed clastic beds ("radiolarian turbidites") with a specific clast composition regarded as volcanogenic in origin. These events provide a powerful means for correlation. Additionally, they prove the allocyclic control of the sedimentary evolution, e.g. by means of the mid-Cretaceous volcanism. Rarely occurring allodapic limestones show a clast composition that strongly differs from the two associations observed in the Upper Cretaceous section. This indicates a pronounced shift in the facial pattern of the former western platform rim (not exposed today) at the end of the Lower Cretaceous.
A drastic change in the sedimentary dynamics of the sharply contrasting Upper Cretaceous was observed, starting in the Middle Cenomanian, which is interpreted as reflecting tectonic and orogenetic processes.
Cenomanian to Coniacian/Santonian: The bulk of the sediment in the Upper Cretaceous section is of clastic origin. Part two of this study deals with the stratigraphic and sedimentological aspects of the clastic facies of the Katafito Formation.
Siliciclastic turbidite successions, introduced by orbitoline-rich mass-flow-deposits (orbitoline horizons), occur excusively in the lower Upper Cretaceous (turbidite intervals of the lower Upper Cretaceous). In the Pindos Mountains and the Peloponnese several different calcareous, siliciclastic and organic-rich turbidite associations could be distinguished. Regional distribution and vertical patterns support the interpretation of submarine fan environments. Analysis of turbidite facies and paleocurrents prove sediment input from the north as well as from unknown terrigeneous sources within the western Apulian platform. Additionally, the abundant volcanoclastic debris in the easternmost outcrops was shed from the eastern Pelagonian Zone.
These phases of redeposition are interpreted as being controlled by tectonism: tectonically-induced falls of relative sea-level caused platform collapses and subsequent terrigeneous supply from attached shelf areas. These events were shown to closely mirror erosive and transgressive events in the eastern Pelagonian Zone.
Coniacian/Santonian to Maastrichtian: In the Late Coniacian to Santonian siliceous and siliciclastic deposition ceased and a carbonate deep-water sedimentary regime developed (Platy Limestone Formation). The third part of this study deals with the litho- and biostratigraphic subdivision of this formation, the analysis of turbidite and microplankton-rich, pelagic facies as well as the correlation of redepositional events. A major task was the application of a consistent biostratigraphic framework based on thin-section analysis. Precise descriptions of planktonic foraminifera can be found in the appendix.
The Upper Santonian to Maastrichtian interval represents a rather uniform carbonate slope (lower slope apron and basin plain), formerly attached to a western platform, which can be inferred from basin-fill facies and thickness trends. Microfacies analysis proves an erosional slope type (by-pass margin). The accumulation of carbonate sediment is due to enhanced periplatform input, i.e. high productivity in the shelf, on one hand, and tectonism, as described in the lower Upper Cretaceous, on the other. Several major redepositional horizons could be defined. The Lower Campanian and the Maastrichtian horizones initiated phases of intensified turbidite shedding (turbidite intervals). These turbidite intervals combined with superimposed small-scale stacking patterns (e.g. thinning-upward successions) are seen as reflecting phases of intensified tectonic activity along the platform-slope margin. The upper and most prominent turbidite interval of the gansseri-zone (Maastrichtian) mirrors the widespread collapse of the internal Hellenide zones and the tilting of the Apulian platform as well. These orogenetic processes with the accompanying paleogeographic changes gave way to the later flysch deposition in the western Hellenides. Terrigeneous supply in the Pindos Basin started in the Upper Maastrichtian.
| Vorwort | 13 | Abkürzungen | 14 | ||
| 1 | Einführung | 15 | |||
| 1.1 | Zielsetzung | 15 | |||
| 1.2 | Paläogeographie und Tektonik | 16 | |||
| 1.2.1 | Allgemeines | 16 | |||
| 1.2.2 | Zur Diskussion des Sedimentbecken-Typs | 16 | |||
| 1.2.3 | Kreide-Fazies und tektonische Ereignisse im Umfeld des Pindos-Beckens | 16 | |||
| 1.3 | Stratigraphie und Lithofazies der Kreide | 20 | |||
| 1.3.1 | Stratigraphie der Kreide: Aufteilung der Arbeit in drei Themenbereiche | 20 | |||
| 1.3.2 | Historisches, Stand der Forschung | 20 | |||
| 1.3.3 | Bisherige Kenntnis der Kreide-Lithofazies der Pindos-Zone | 20 | |||
| 1.3.3.1 | Unter- und tiefere Oberkreide | 20 | |||
| 1.3.3.2 | Höhere Oberkreide (karbonatische Sedimente) | 23 | |||
| 2 | Arbeitsmethodik und Datenpräsentation | 23 | |||
| 2.1 | Lage des Untersuchungsgebietes mit Profil- und Aufschlusspunkten | 23 | |||
| 2.2 | Profildokumentation | 23 | |||
| 2.3 | Biostratigraphie | 25 | |||
| 2.3.1 | Radiolarien | 25 | |||
| 2.3.2 | Planktonische Foraminiferen | 25 | |||
| 2.3.3 | Kalkiges Nannoplankton | 27 | |||
| 2.4 | Sedimentologisch-geochemische Auswertungen | 27 | |||
| 3 | Ergebnisse: Sedimentologie, Events und Biostratigraphie | 28 | |||
| 3.1 | Lithostratigraphie – Gliederung der Kreide und lithostratigraphische Nomenklatur | 28 | |||
| 3.2 | Radiolarit-Fazies der Katafito-Formation (Unter- bis tiefe Oberkreide) | 30 | |||
| 3.2.1 | Dokumentation des Profils 9 Katafito (Unterkreide-Turon; Pindos-Gebirge) | 30 | |||
| 3.2.2 | Sedimentgesteine und Fazies | 36 | |||
| 3.2.2.1 | Lithologische Zusammensetzung der Radiolarit-Fazies | 36 | |||
| 3.2.2.2 | Grüne Horizonte und Schwarzschiefer | 36 | |||
| 3.2.2.3 | Detritische Einschaltungen – spezielle Mineral- und Klastenassoziationen | 39 | |||
| 3.2.2.4 | Zusammenfassung Grüner Horizonte und sedimentärer Charakteristika | 40 | |||
| 3.2.3 | Radiolarien – Ergebnisse der mikrobiostratigraphischen Auswertung | 40 | |||
| 3.2.4 | Zusammenfassung und Diskussion | 43 | |||
| 3.3 | Klastische Fazies der Katafito-Formation (tiefe Oberkreide) | 44 | |||
| 3.3.1 | Orbitolinenhorizonte: Karbonatisch-klastische Fazies | 44 | |||
| 3.3.1.1 | Übersicht zu Verbreitung und Sedimentologie | 47 | |||
| 3.3.1.2 | Zur Mikrofazies und Mikropaläontologie | 47 | |||
| 3.3.1.3 | Dünnschliff-petrographische und mikrofazielle Dokumentation (Beispiele) | 48 | |||
| 3.3.1.4 | Anmerkungen zur Mikrobiostratigraphie | 49 | |||
| 3.3.1.5 | Anmerkungen zur stratigraphischen Erosion | 50 | |||
| 3.3.2 | Klastische Fazies in der internen Pindos-Zone (Ostpeloponnes) | 51 | |||
| 3.3.2.1 | Lithoklasten und Petrographie der grobkörnigen Turbidite | 51 | |||
| 3.3.2.2 | Vulkanite – petrographischer Überblick | 52 | |||
| 3.3.2.3 | Deutung der ostpeloponnesischen Verhältnisse | 53 | |||
| 3.3.3 | Siliziklastische Turbidit-Fazies | 53 | |||
| 3.3.3.1 | Turbiditassoziationen | 53 | |||
| 3.3.3.2 | Sedimentstrukturen und Fazies der siliziklastischen Turbidite | 54 | |||
| 3.3.3.3 | Spektrum des terrigenen und karbonatischen Detritus | 55 | |||
| 3.3.3.4 | Dünnschliff-petrographische Dokumentation einiger Sandsteintypen (Beispiele) | 56 | |||
| 3.3.3.5 | Bio-lithostratigraphische und regionale Verbreitung | 58 | |||
| 3.3.4 | Paläoströmungsmuster und Bedeutung der Turbiditfazies der tieferen Oberkreide | 58 | |||
| 3.3.4.1 | Bisherige Kenntnis | 58 | |||
| 3.3.4.2 | Ergebnisse dieser Arbeit | 59 | |||
| 3.3.5 | Zusammenfassung und Diskussion | 60 | |||
| 3.4 | Pindos-Plattenkalk-Formation (höhere Oberkreide) | 61 | |||
| 3.4.1 | Dokumentation des Profils 23 Katafito (Pindos Gebirge) | 61 | |||
| 3.4.2 | Bio-lithostratigraphische Kurzcharakterisierung der Pindos-Plattenkalk-Formation | 70 | |||
| 3.4.3 | Feinkörnige Fazies: Pelagische Biomikrite und Mudturbidite | 71 | |||
| 3.4.3.1 | Pelagische Biomikrite | 71 | |||
| 3.4.3.2 | Mudturbidite | 71 | |||
| 3.4.4 | Planktonische Foraminiferen: Events und Mikrobiostratigraphie | 72 | |||
| 3.4.4.1 | Bioevents – Foraminiferenvergesellschaftungen | 73 | |||
| 3.4.4.2 | Mikrobiostratigraphische Datierung der Profile | 73 | |||
| 3.4.5 | Grobkörnige Fazies: Arenitische bis ruditische Mass-flow-Ablagerungen | 73 | |||
| 3.4.5.1 | Turbiditfazies | 74 | |||
| 3.4.5.2 | Debris- und Mud-flow-Fazies | 74 | |||
| 3.4.6 | Siliziklastische Ablagerungen der Rigani-Schichten | 74 | |||
| 3.4.7 | Zusammenfassung des umgelagerten Bio- und Lithoklastenspektrums | 76 | |||
| 3.4.7.1 | Santon bis tieferes Maastricht | 76 | |||
| 3.4.7.2 | Höheres Maastricht (ab gansseri-Zone) | 76 | |||
| 3.4.7.3 | Anmerkungen zur stratigraphischen Erosion | 76 | |||
| 3.4.8 | Umlagerungsereignisse und Turbiditzyklen | 76 | |||
| 3.4.8.1 | Definition von Umlagerungsereignissen | 76 | |||
| 3.4.8.2 | Turbiditzyklen | 78 | |||
| 3.4.8.3 | Mächtigkeitsentwicklung und Paläoströmungsmuster | 78 | |||
| 3.4.9 | Zusammenfassung und Diskussion | 81 | |||
| 4 | Literatur | 84 | |||
| Anhang | 89 | ||||
| A. | Bio- und Lithoklasten-Assoziationen | 90 | |||
| 1. | Santon bis Maastricht (Pindos-Plattenkalk-Formation) | 90 | |||
| 2. | Analyse der Erosion im Liefergebiet im Santon bis Maastricht (Beispiele) | 95 | |||
| 3. | Tiefere Oberkreide (Orbitolinenhorizonte) | 96 | |||
| B. | Plankton-Biostratigraphie | 98 | |||
| 1. | Planktonische Foraminiferen | 98 | |||
| 2. | Radiolarien | 101 | |||
| C. | Tafeln zur Mikropaläontologie und Mikrofazies | 104 | |||
| D. | Grüne Horizonte und Schwarzschiefer | 116 | |||
| 1. | Geochemische Daten (Leco-Analyse) | 116 | |||
| 2. | Tabellarische Zusammenstellung der Schwarzschieferlagen im Profil 9 Katafito | 117 | |||
| E. | Profildokumentation (1:500) | 118 | |||
| F. | Proben- und Fossildatensatz | 141 | |||
| G. | Analyse von Paläoströmungen | 154 | |||
| H. | Literaturdaten | 156 | |||
| Copyright © 2009 Verlag Dr. Friedrich Pfeil |