A coral-microbialite patch reef from the late jurassic (florigemma-Bank, Oxfordian) of NW Germany (Süntel mountains)

Helm, Carsten; Schülke, Immo

doi:10.1007/bf02537012

Cited by 38 publications

(21 citation statements)

References 57 publications

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“…Dupraz and Strasser (1999), who examined the encrustations of Oxfordian coral reefs in the Jura, correlated the Bacinella-Lithocodium association with episodes of relatively high coral diversity. Bacinella and Lithocodium have also been identiWed in the microbial crusts associated with coral and sponge reefs of the Late Jurassic (e.g., Helm and Schülke 1998;Dupraz and Strasser 1999;Schmid and Leinfelder 1996;Olivier et al 2004;Shiraishi and Kano 2004). This may suggest that palaeoecological conditions for Bacinella-Lithocodium bearing oncoids were analogous.…”

Section: Classiwcationmentioning

confidence: 97%

Oncoid growth and distribution controlled by sea-level fluctuations and climate (Late Oxfordian, Swiss Jura Mountains)

Védrine

Strasser

Hug³

2007

Facies

100

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Abundant lagoonal oncoids occur in the Late Oxfordian Hauptmumienbank Member of the Swiss Jura Mountains. Four oncoid types are observed in the studied sections and classiWed according to the oncoid surface morphology, the structure and composition of the cortex, and the texture and fauna of the encasing sediment. Micritedominated oncoids (types 1 and 2) have a smooth surface. Type 1 has a rather homogeneous cortex and occurs in moderate-energy environments. Type 2 presents continuous or discontinuous micritic laminae. It is associated with a low-diversity fauna and occurs in high-energy facies. Bacinella and Lithocodium oncoids (types 3 and 4) display a lobate surface. They are dominated by microencrusters (Bacinella irregularis and Lithocodium aggregatum) and are found in low-energy facies. The stratigraphic and spatial distribution of these oncoid types shows a correlation with the sequence-stratigraphic evolution of the studied interval, and thus with relative sea-level Xuctuations. It can be shown that these sea-level Xuctuations were controlled by orbital cycles with 100-and 20-kyr periodicities. At the scale of 100-and 20-kyr sequences, types 1 and 2 oncoids are preferentially found around sequence boundaries and in transgressive deposits, while types 3 and 4 oncoids are preferentially found around maximum Xoodings and in highstand deposits. This implies that changes of water energy and water depth were direct controlling factors.Discrepancies in oncoid distribution point to additional controlling factors. Platform morphology deWnes the distribution and type of the lagoon where the oncoids Xourished. A low accumulation rate is required for oncoid growth. Additionally, humidity changes in the hinterland act on the terrigenous inXux, which modiWes water transparency and trophic level and thus plays a role in the biotic composition and diversity in the oncoid cortex.

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Section: Classiwcationmentioning

confidence: 97%

Oncoid growth and distribution controlled by sea-level fluctuations and climate (Late Oxfordian, Swiss Jura Mountains)

Védrine

Strasser

Hug³

2007

Facies

100

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“…In many instances the reefal character of these coral assemblages is clear. The northernmost occurrences are in northern Germany (Bertling, 1993;Helm and Schülke, 1998) but, Helm and Schülke (2003), Helm et al (2001Helm et al ( , 2003a and Reuter et al (2001) indicate that these may be Middle Oxfordian. Interestingly, the reefal assemblages typical of the Middle Oxfordian in northern latitudes are found at lower latitudes in the Upper Oxfordian of eastern France (Lorraine) and Switzerland .…”

Section: Distribution Of Coral Reefsmentioning

confidence: 99%

Paleoclimatic control of biogeographic and sedimentary events in Tethyan and peri-Tethyan areas during the Oxfordian (Late Jurassic)

Cecca¹,

Martin-Garin²,

Marchand³

et al. 2005

Palaeogeography, Palaeoclimatology, Palaeoecology

117

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The paleobiogeographical distribution of Oxfordian ammonites and coral reefs in northern and Central Europe, the Mediterranean area, North and East Africa, and the Middle East and Central Asia is compared with the distribution in time and space of the most important lithofacies. Interest in the Oxfordian is focused on changes in facies and in biogeographical patterns that can be interpreted as the results of climatic events. Paleotemperature trends inferred from oxygen isotopes and paleoclimatic simulations are tested against fossil and facies data. A Late Callovian-Early Oxfordian crisis in carbonate production is indicated by the widespread absence of Lower Oxfordian reefal formations. There is a gap (hiatus) in deposition on epicontinental platforms, with Middle Oxfordian deposits resting paraconformably on Upper Callovian, while shales accumulated in adjacent intracratonic basins. Simultaneously, in Mediterranean Tethys, radiolarites accumulated in deep troughs while Rosso Ammonitico facies formed on pelagic swells. However, deposition on swells was also discontinuous with numerous gaps (hiatuses) and sequences that are much reduced in thickness. Middle Callovian deposits are generally overlain by Middle Oxfordian limestones. The dearth of carbonates is consistent with a cooling event lasting about 1 My. By the middle Oxfordian a warming, leading to bgreenhouseQ type conditions, is suggested on the basis of both biogeographical (mostly coralreef distribution) and geochemical data. Carbonates spread onto an extensive European platform while radiolarites reached a maximum development in the Mediterranean Tethys. Two distinct latitudinal belts, with seemingly different accumulation regimes, are therefore inferred. Similar latitudinal belts were also present in the late Oxfordian, when carbonates were widespread. The distribution of reefal facies in the late Oxfordian-early Kimmeridgian fits relatively well with GCMs simulations that imply low rainfall in the Tethyan Mediterranean area and slightly higher precipitation in central and northern Europe. Local salinity variations, reflecting more arid or humid conditions, may bias the paleotemperature signal inferred from

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“…These abiologic explanations cannot be excluded and therefore the use of carbonaceous matter in Akilia samples as a tracer for ancient life is ambiguous. Arp et al 2005), marine non-cyanobacterial stromatolites of the Schwarzjura Group (Arp et al 2004), marine reefal microbialite crusts (Oxfordian Reefs of the "Korallenoolith"; Helm & Schülke 1998, Betzler et al 2006, freshwater oncoids (Berriasian "Purbeck" deposits; Dragastan & Richter 2001, Arp & Mennerich 2008, and, relatively recently discovered , deeper-marine seep carbonates of the Lower Carboniferous (Stop 4: Iberg) (Table 1). Present-day forming microbialites are restricted to tufa stromatolites of karst-water creeks (e. g., Westerhöfer Creek; , discharging from aquifers largely of Mesozoic limestone formations.…”

Section: Do Calcium-sensitive Dyes Bind To Specific Proteins Within Tmentioning

confidence: 99%

Geobiology of Stromatolites

Reitner¹,

Quéric²,

Reich³

2008

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A coral-microbialite patch reef from the late jurassic (florigemma-Bank, Oxfordian) of NW Germany (Süntel mountains)

Cited by 38 publications

References 57 publications

Oncoid growth and distribution controlled by sea-level fluctuations and climate (Late Oxfordian, Swiss Jura Mountains)

Oncoid growth and distribution controlled by sea-level fluctuations and climate (Late Oxfordian, Swiss Jura Mountains)

Paleoclimatic control of biogeographic and sedimentary events in Tethyan and peri-Tethyan areas during the Oxfordian (Late Jurassic)

Geobiology of Stromatolites

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