radiolaria - Marum

Bibliography - 1991 Radiolaria 14
published in collaboration with the author (Guex and Davaud 1982,
1984, 1986). The last version of this program will be referred to as
"DV-86". The most recent program, named "BioGraph", was
developed on an IBM microcomputer by Savary (Savary and Guex
1991). This very efficient program is described in Chapter 6. It is
used to solve most of the difficult problems presented in this book.
Gutschick, R.C. & Sandberg, C.A. 1991a. Upper
Devonian biostratigraphy of Michigan Basin. In: Early
sedimentary evolution of the Michigan Basin. (Catacosinos,
P.A. & Daniels, P.A.J., Eds.), vol. 256. Geological Society
of America, special Papers, pp. 155-179.
The Late Devonian Michigan Basin was floored by the Middle and
Upper Devonian Squaw Bay Limestone, which was deposited during
the downwarping that produced the basin within a former Middle
Devonian carbonate platform. The Squaw Bay comprises three beds,
each having a different conodont fauna. The two upper beds,
deposited during the transitans Zone, have different conodont
biofacies that reflect this deepening. The basin was largely filled by
the deep-water, anaerobic to dysaerobic, organic-rich, black Antrim
Shale, which has a facies relationship with the prodeltaic, greenish
gray Ellsworth Shale that prograded into the basin from the west. The
Upper Devonian (Frasnian to Famennian) Antrim Shale is divided into
four members, from base to top: the Norwood, Paxton, Lachine, and
upper members. These members are more or less precisely dated by
conodonts. The Norwood was deposited during the transitans Zone to
Ancyrognathus triangularis Zone, and the Paxton was deposited from
that zone probably through the linguiformis Zone at the end of the
Frasnian. The overlying Lachine was deposited during the early
Famennian and has yielded faunas of the Upper crepida and Lower
rhomboidea Zones. Only the lower part of the upper member is
exposed, and near Norwood, Michigan, it yielded conodonts of the
Lower marginifera Zone. The widespread Famennian floating plant
Protosalvinia (Foerstia) has not yet been found in outcrops of the
Antrim, and should not be expected to occur except in the upper
member or highest part of the Lachine Member. Its range in terms of
conodont zones is from the Upper trachytera Zone through the Lower
expansa Zone and possibly into the Middle expansa Zone. One known
subsurface occurrence might be datable as rhomboidea or Lower
marginifera Zone, depending on gamma ray correlations to outcrops.
Black shale deposition ended when the Late Devonian mud delta of
the Bedford Shale prograded across the Michigan Basin from the east
and then retreated as the regressive Berea Sandstone was being
deposited during the major eustatic sea-level fall that ended the
Devonian. The Bedford was deposited during the Upper expansa to
Lower praesulcata Zones, and the Berea was deposited during the
Middle to Upper praesulcata Zones. Both formations contain the
spore Retispora lepidophyta, which is a global indicator of latest
Devonian age.
Gutschick, R.C. & Sandberg, C.A. 1991b. Late
Devonian history of Michigan Basin. In: Early sedimentary
evolution of the Michigan Basin. (Catacosinos, P.A. &
Daniels, P.A.J., Eds.), vol. 256. Geological Society of
America, special Papers, pp. 181-202.
The Upper Devonian sequence in the Michigan Basin is a
westward extension of coeval cyclical facies of the Catskill deltaic
complex in the Appalachian basin. Both basins and the intervening
Findlay arch express the tectonic and sedimentational effects of
foreland compression and isostatic compensation produced by the
Acadian orogeny. The Late Devonian Michigan Basin formed as one of
several local deeps within the long Eastern Interior seaway that
separated the North American craton, backboned by the
Transcontinental arch, on the west from the Old Red continent,
Avalon terrane (micro-plate), and possibly northwest Africa on the
east. Basin development began in the late Middle Devonian (late
Givetian varcus Zone) with subsidence of a shallow-water carbonate
platform formed by rocks of the Traverse Group. Subsidence was
contemporaneous with Taghanic onlap of the North American craton.
During subsidence, a thin transitional sequence of increasingly
deeper water limestones separated by hardgrounds was deposited in
the incipient Michigan Basin during the latest Givetian to earliest
Frasnian disparilis to falsiovalis Zones. Deposition of this sequence
culminated during the early Frasnian transitans Zone with a
calcareous mudstone bed at the top of the Squaw Bay Limestone.
Subsidence was followed by a 12-m.y.-long Late Devonian episode of
slow, hemipelagic, basinal sedimentation of organic black muds that
formed the Antrim Shale, interrupted basinwide only by deposition of
its prodeltaic Paxton Member. Westward, the basinal Antrim black
muds intertongued with greenish gray, deltaic and prodeltaic muds of
an eastward-prograding delta platform formed by the Ellsworth
Shale. Basinal black shale deposition ceased in latest Devonian (late
Famennian Lower praesulcata Zone) time, when the Bedford deltaic
complex prograded westward, completely filling the Antrim Basin and
even covering part of the older Ellsworth deltaic complex on the
west. As sea level was lowered eustatically near the end of the
Devonian, the regressive Berea Sandstone terminated deltaic
deposition. After an Early Mississippian erosional episode,
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widespread deposition of the unconformably overlying Lower
Mississippian Sunbury Shale began during the next transgression,
associated with a major eustatic rise in the Lower crenulata Zone.
Haslett, S.K. & Robinson, P.D. 1991.
Micropaleontology notebook: detection of Radiolaria in the
field. J. Micropaleont., 10/1, 22.
Radiolaria can be preserved in all types of marine sedimentary
rocks, the method for their extraction being dependent on the
mineralogy of the radiolarian test and the nature of the rock-type in
which they occur. In the past radiolaria could only be viewed in thin
section (Hinde, 1890; Hinde & Fox, 1895), with no method of
detecting the presence of radiolaria prior to sectioning. Modern
extraction techniques are normally laboratory based and use
hazardous chemicals, therefore it is advantageous to establish the
radiolarian content of the sample before collection and
transportation back to the laboratory. This can be achieved in a
number of ways: non-lithified sediments, siliceous rock-types,
limestone, phosphate nodules and argillites
Hernández-Molina, F.J., Sandoval, J., Aguado,
R., O'Dogherty, L., Comas, M.C. & Linares, A.
1991. Olistoliths from the Middle Jurassic in Cretaceous
materials of the Fardes formation. Biostratigraphy (Subbetic
Zone, Betic Cordillera). Rev. Soc. geol. España, 4/1-2, 79-
104.
The Middle Jurassic olistoliths studied are found within
Cretaceous materials of the south-eastern part of the Montes
Orientales region (province of Granada, Betic Cordillera), specifically
in the Rio Fardes sector. The cretaceous materials are here
characterized by pelagic and hemipelagic facies with abundant
turbidite and olistostrome insertions in a deep basin marine
environment (Middle Subbetic), bounded to the SE by a pelagic ridge
(Internal Subbetic). The transition between the two domains was an
area with active paleoslopes which facilitated both the exposure and
denudation of Jurassic and Cretaceous materials and the
development of a clear synsedimentary tectonics (slumps and
olistostromes). Paleocurrents show that the source area of
materials forming the thickest beds was located towards the S-SW,
though for the thinner beds they are more widely dispersed.
The sections under study have been dated by means of
calcareous nannoplankton, planktonic foraminifera and radiolaria.
The calcareous nannofossil assemblages enable us to distinguish
Sissingh's zones CC-9, CC-10 and CC-13 for the Lower
Cenomanian-Coniacian, which in turn determines the position of the
Jurassic olistoliths within the sections. The precise age of the
materials where the large-sized olistoliths are embedded is
Coniacian (Marthasterites furcatus zone of calcareous
nannoplankton).
Olistoliths from the Middle Jurassic are often sufficiently
exposed and stratified to allow sampling level by level and the
establishing of a detailed biostratigraphy. After a study of the
ammonite fauna collected in two olistoliths we were able to
distinguish the Murchisonae and Concavum zones in the Aalenian,
and the Discites, Laeviuscula, Sauzei and Humphriesianum zones in
the Bajocian.
In those areas with S-SW paleocurrents Aalenian materials are
not found, but the Bajocian materials of some nearby sectors
belonging to the Internal Subbetic have a similar lithology and faunal
content.
Hollis, C.J. & Hanson, J.A. 1991. Well-preserved late
Paleocene Radiolaria from Tangihua Complex, Camp Bay,
eastern Northland. Tane, 33, 65-76.
A sparse but very well-preserved radiolarian fauna has been
obtained from interpillow limestone in the allochthonous Tangihua
Complex at Camp Bay, northwest of Whangaroa Harbour. A Late
Paleocene age (58-62 Ma) is probable; primarily because of the
presence of Buryella cf. tetradica Foreman, a variant of B. tetradica
known only from the Paleocene, and the absence of Early Paleocene
or latest Paleocene-Eocene index species. This is the first
unequivocal record of Tertiary fossils from Tangihua sediments. The
assemblage suggests upper-mid bathyal, warm-temperate conditions
of deposition.
The good state of preservation and the presence of established
index species show that radiolarians have potential for improving
age control and clarifying the depositional conditions of sediments
associated with Tangihua igneous massifs.
Hull, D.M. 1991. Upper Jurassic radiolarian
biostratigraphy of the lower member of the Taman
Formation, east-central Mexico and of volcanopelagic strata