Evidence from phytoplankton associations for causes of black shale formation in epicontinental seas

1989 ◽  
Vol 1989 (11) ◽  
pp. 671-682 ◽  
Author(s):  
Michael Prauss ◽  
Walter Riegel
Keyword(s):  
Black Shale ◽  
Shale Formation

scholarly journals Black shale formation environment and its control on shale oil enrichment in Triassic Chang 7 Member, Ordos Basin, NW China

2021 ◽  
Vol 48 (6) ◽  
pp. 1304-1314
Author(s):  
Bin ZHANG ◽  
Zhiguo MAO ◽  
Zhongyi ZHANG ◽  
Yilin YUAN ◽  
Xiaoliang CHEN ◽  
...  
Keyword(s):  
Black Shale ◽  
Ordos Basin ◽  
Shale Oil ◽  
Nw China ◽  
Shale Formation

scholarly journals Erratum to “A Perspective on Stratigraphic, Vertically-Upward “Displacements or Dislocations” of Conodont-Elements: An Example From the Upper Devonian, Pre-Lithified, Black Shales of the Chattanooga Shale Formation In Tennessee, USA” ...

2019 ◽  
Vol 9 (1) ◽  
pp. 14
Author(s):  
Michael Iannicelli
Keyword(s):  
Black Shale ◽  
Environmental Chemistry ◽  
Black Shales ◽  
Photic Zone ◽  
Marine Organic Matter ◽  
Chattanooga Shale ◽  
Shale Formation ◽  
Organic Matter Biomarkers ◽  
Reference Section ◽  
Made In

Even though the author already incorporated the citation of Sinninghe-Damste & Schouten (2006) into the text of the paper, the author regrets having failed to include their full citation within the Reference Section of my above paper which is: Sinninghe-Damste, J. S. & Schouton, S. (2006). Biological markers for anoxia in the photic zone of the water column. In, Volkman, J. K. (ed.), Marine Organic Matter: Biomarkers, Isotopes and DNA, (pp. 127 – 163). The Handbook of Environmental Chemistry, vol. 2N. Springer: Berlin and Heidelberg. https://doi.org/10.1007/698_2_005 The author also needs to paraphrase a statement made in the last three lines of the 2nd paragraph on page 40 where it reads as: “Thus, we may conclude here that paleo-upfreezing of any conodont-element(s) originally buried in the pre-lithified, light-colored shale occurred in order to account for their presence in black shale”. Instead, in lieu of that statement, it should read as “At this point in time of the study, we may tentatively conclude here while completely concluding later in the study, that conodont-elements originally existing in the underlying, pre-lithified, light-colored shale, had to paleo-upfreeze vertically upward into pre-lithified, black shale sediment in order to account for their presence in lithified black shale”.

Redox sensitivity of P cycling during marine black shale formation: Dynamics of sulfidic and anoxic, non-sulfidic bottom waters

2008 ◽  
Vol 72 (15) ◽  
pp. 3703-3717 ◽  
Author(s):  
C. März ◽  
S.W. Poulton ◽  
B. Beckmann ◽  
K. Küster ◽  
T. Wagner ◽  
...  
Keyword(s):  
Black Shale ◽  
P Cycling ◽  
Formation Dynamics ◽  
Bottom Waters ◽  
Shale Formation ◽  
Redox Sensitivity

Arctic black shale formation during Cretaceous Oceanic Anoxic Event 2

Geology ◽  
2014 ◽  
Vol 42 (9) ◽  
pp. 799-802 ◽  
Author(s):  
Marc Lenniger ◽  
Henrik Nøhr-Hansen ◽  
Len V. Hills ◽  
Christian J. Bjerrum
Keyword(s):  
Black Shale ◽  
Oceanic Anoxic Event ◽  
Oceanic Anoxic Event 2 ◽  
Anoxic Event ◽  
Shale Formation

scholarly journals A regional ocean circulation model for the mid-Cretaceous North Atlantic Basin: implications for black shale formation

2010 ◽  
Vol 6 (5) ◽  
pp. 2371-2421 ◽  
Author(s):  
R. P. M. Topper ◽  
J. Trabucho Alexandre ◽  
E. Tuenter ◽  
P. Th. Meijer
Keyword(s):  
Ocean Circulation ◽  
Black Shale ◽  
North Atlantic ◽  
Initial Conditions ◽  
Regional Model ◽  
Black Shales ◽  
Global Ocean ◽  
Atlantic Basin ◽  
North Atlantic Basin ◽  
Shale Formation

Abstract. High concentrations of organic matter accumulated in marine sediments during Oceanic Anoxic Events (OAEs) in the Cretaceous. Model studies examining these events invariably make use of global ocean circulation models. In this study, a regional model for the North Atlantic Basin during OAE2 at the Cenomanian-Turonian boundary is developed. A first order check of the results is performed by comparison with the results of a recent global Cenomanian CCSM3 run from which boundary and initial conditions were obtained. The regional model is able to maintain tracer patterns and to produce velocity patterns similar to the global model. The sensitivity of basin tracer and circulation patterns to changes in the geometry of the connections with the global ocean is examined with three experiments with different bathymetries near the sponges. Different geometries turn out to have little effect on tracer distribution, but do affect circulation and upwelling patterns. The regional model is also used to test the hypothesis that ocean circulation may be behind the deposition of black shales during OAEs. Three scenarios are tested which are thought to represent pre-OAE, OAE and post-OAE situations. Model results confirm that Pacific intermediate inflow together with coastal upwelling can have enhanced primary production during OAE2. A low sea level in the pre-OAE scenario can inhibit large scale black shale formation, as can the opening of the Equatorial Atlantic Seaway in the post-OAE scenario.

scholarly journals Cambrian–Silurian stratigraphy of Børglum Elv, Peary Land, eastern North Greenland

1977 ◽  
Vol 82 ◽  
pp. 1-48
Author(s):  
R.L Christie ◽  
J.S Peel
Keyword(s):  
Black Shale ◽  
Lower Cambrian ◽  
Late Ordovician ◽  
Dolomitic Limestone ◽  
Carbonate Mounds ◽  
Middle Ordovician ◽  
Clastic Rocks ◽  
Shale Formation ◽  
Lower Palaeozoic ◽  
North Greenland

A sequence of Lower Palaeozoic carbonate and clastic rocks is described from Børglum Elv, Peary Land, eastem North Greenland, and briefly compared to Lower Palaeozoic sections elsewhere in Greenland and in Spitsbergen. Lower Cambrian clastic rocks of the Buen Formation are followed by dolomite of the Lower Cambrian Brønlund Fjord Formation (125 m). Succeeding dolomite and dolomitic limestone of the Wandel Valley Formation (320 m) of Early to Middle Ordovician age are overlain by limestone of the Børglum River Formation (430 m) of Middle to Late Ordovician age. Un-narned Early Silurian dolomite and limestone formations (150 m and 320 m respectively) are followed by an un.narned Middle Silurian black shale formation (c. 100 m) and at least 800 m of a late Middle Silurian and younger un-named flysch formation. Carbonate mounds, originating in the highest beds of the un-named Silurian limestone formation, occupy stratigraphic levels through the overlying black shale formation and into the flysch formation.

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