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The Unique Devonian of Immouzer-Du-Kandar (Middle Atlas Basement) – Biostratigraphy, Faunas, and Facies Development

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  • Devonian of Immouzer-du-Kandar

The unique Devonian of Immouzer-du-Kandar
(Middle Atlas basement) – biostratigraphy, faunas, and facies development

ZHOR SARAH ABOUSSALAM, RALPH THOMAS BECKER,

JULIA RICHTER, SVEN HARTENFELS,

AHMED EL HASSANI & STEPHAN EICHHOLT

Fig. 1: View (from the hill at Douar Ahmed-ben-Mellouk) on Devonian exposures of Immouzer-du-Kandar (hill rising from Chabat el Jenanet, Sections C2 and C3 of CYGAN et al. 1990), our Section C4, with outcrop of the lower Emsian conglomerate (Chabat Jenanet Formation) along and above the track, faulted upper Emsian to lower Givetian limestones in the lower slope (new Ahmed-ben-Mellouk Formation), the reef breccia forming a small terrace ca. 2/3 upwards, and the Famennian upper slope (new Chabat el Hallouf Formation, Section C5) towards the top. The slope to the left (NNE) is occupied by Triassic red beds. Section numbers are marked in circles.

1. Introduction

Mesozoic Middle Atlas, with the best and most important outcrops in the tectonic window
The Middle Atlas divides the Moroccan (“boutonnière”) at Immouzer-du-Kandar, ca.
Meseta into the Western and Eastern Meseta, 40 km S of Fès. The wooded Jebel Kandar to which differ strongly in the Devonian in terms the SW is a more than 1600 m high mountain of facies and synsedimentary structural built of Jurassic strata (Fig. 2). Fossiliferous

  • geology (e.g., overviews of EL HASSANI & Ordovician
  • to
  • Lower
  • Carboniferous

BENFRIKA 1995, 2000). There is restricted formations crop out to the NW, from Dour knowledge of the Palaeozoic basement of the Rouda towards the SE, the Chabat el Jenanet,

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and then towards the Chabat al Sitout (Fig. 4) 2006 for overview)). There are coarse The Devonian litho- and biostratigraphy of the conglomerates and slump masses with “alien” area has been established by the CHARRIÈRE & (e.g., TAHIRI et al. 2017) magmatic rocks, RÉNAULT (1989) and CYGAN et al. (1990; Fig. which must have been derived from a proximal 3). Comparisons with other Meseta regions Neoproterozoic to Lower Palaeozoic source. showed from the beginning that the succession This differs considerably from the basement of includes many unique sedimentological units, other Meseta regions. Therefore, any new

  • faunas and floras (FAIRON-DEMARET & stratigraphical,
  • sedimentological,

REGNAULT 1986), which isolate it both from palaeontological, and geochemical data add to the closest Devonian of the East-Central the knowledge of a crucial segment of Meseta Meseta (e.g., PIQUE & MICHARD 1981; Azrou- palaeogeography and tectonics. However, the Khenifra nappes) and from the predominantly Immouzer-du-Kandar Devonian may represent siliciclastic Eastern Meseta e.g., at Tazekka, a transported, allochthonous unit, as the nappes which is separated by the Tazekka-Bsabis- of the Azrou to Khenifra region. Bekrit Fault Zone (see HOEPPFNER et al. 2005,

Fig. 2: Position of the Jurassic Jebel Kandar and the Jenanet succession (red dot for Fig. 1) in the SW corner of topographic sheet, 1: 50 000, NI-30-VIII-3c, Sefrout.

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By detailed section logging, conodont and OUARHACHE (1987): Unpublished thesis on macrofauna sampling, as well as microfacies the Palaeozoic to Triassic at the NW margin analyses in the last ca. 10 years, we can of the Middle Atlas S of Fés. significantly refine the local litho- and

CHARRIÈRE (1989) and CHARRIÈRE

&biostratigraphy and provide a more precise RÉGNAULT (1989): Principles of Devonian reconstruction of facies changes, sea-level, and Carboniferous litho- and biostratigraphy and local influences of global events, for of Immouzer-du-Kandar. example around the Emsian-Eifelian, middle- CHARRIÈRE (1990): Unpublished Ph.D. upper Givetian, and Frasnian-Famennian Thesis on the Hercynian evolution of the boundaries. The studied sections begin in the Middle Atlas basement, with detailed data for branching valley of Chabet el Jenanat and Immouzer-du-Kandar. ascend the western slope of the hill just to SE, WILLEFERT & CHARRIÈRE (1990): Detailed reaching up to the crest (Figs. 1, 2, 4; at x = description of Ordovician and Silurian litho541.8, y = 352.3; GPS N33°45´58.4´´, and graptolite biostratigraphy. W4°56´50.9´´). There are numerous normal

CYGAN

  • et
  • al.
  • (1990):
  • Conodont

faults, which offset especially the upper biostratigraphy of Emsian to lower Frasnian Emsian to Givetian succession at close units at Immouzer-du-Kandar and their distance (Fig. 1). These had to be respected in significance for the understanding of the order to avoid mistakes in the small-scale sedimentary evolution and palaeogeography

  • lateral correlations.
  • of the region.

RACHEBEUF (1990a, 1990b): Record of the

chonetids Ctenochonetes robardeti and Plicanoplica carlsi from lower Emsian grey

2. Research History

HORON (1954): First (unpublished) report on shales of Immouzer-du-Kandar. fossiliferous Silurian (with graptolites) to OUARHACHE et al. (1991): Records of Upper Lower Devonian (with brachiopods) strata at Viséan foraminifers, calcareous algae Immouzer-du-Kandar, followed by a Viséan (Koninckopora), and “pseudo-algae”, such as transgression.

Palaeoberesella, Kamaena, Stacheia, and

CHARRIÈRE & RÉGNAULT (1983) and Aoujgalia.

  • CHARRIÈRE et al. (1984): Preliminary notes on
  • EL HASSANI & BENFRIKA (1995, 2000):

the Immouzer-du-Kandar Devonian litho- and Overviews of the Devonian of the Moroccan

  • biostratigraphy.
  • Meseta, including a summary for the Middle

BRICE et al. (1984): Description and Atlas basement. biostratigraphic dating of Emsian, supposed BERKHLI (1999): Discussion of the

  • Frasnian, and upper Famennian brachiopods.
  • foraminifer age of Viséan limestones at

FAIRON-DEMARET & RÉGNAULT (1986): Immouzer-du-Kandar. Description of Lower and Middle Devonian BERKHLI et al. (2000): Brief discussion of the plant remains, with implications for microfacies of Upper Viséan limestones of stratigraphy (Fig. 3) and palaeobiogeography. Immouzer-du-Kandar in the frame of a RÉGNAULT & CHAUVEL (1987): Description general discussion of Lower Carboniferous of the first Lower Devonian carpoid of sedimentologie and geodynamics of the NE Morocco from the Aïn el Beida Formation, Meseta. representing probably a new (un-named) SARTENAER (2000): Re-assignment of

  • genus of the Anomalocystitida (Mitrata).
  • supposed Planovatirostrum sp. described by

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BRICE et al. (1984) to the new genus of sediments with a terrestrial, coastal, Phacoiderhynchus. siliciclastic inner shelf, carbonate platform, JANSEN (2001): Brief comments on some of seamount, and deep pelagic origin (compare the Pragian brachiopods (Euryspirifer) CHARRIÈRE & RÉGNAULT 1989, tab. 1). The

  • described by BRICE et al. (1984).
  • presence of several coarse reworking units

MICHARD et al. (2008): Reference to the proves significant synsedimentary tectonic Chabat Jenanat conglomerate with reworked movements and active, steep fault scarps in granites, ignimbrites, Ordovician quartzites, the source region of material, from where

  • and Silurian slates.
  • mass flows moved downwards. The deep

GERRIENE et al. (2010): Reference to the erosion into Neoproterozoic basement and the possible occurrence of the aneurophytalean perfect rounding of pebbles show that an genus Rellimia in the “plant shale” at adjacent island must have existed, where

  • Immouzer-du-Kandar.
  • material was constantly moved in fluviatile or

BECKER (2012): Illustration of the Eovariscan coastal environments, prior to transport and breccia at Immouzer-du-Kandar, as an downslope re-deposition. Parts of the example for double reworking. BECKER & ABOUSSALAM (2014): Brief topographic high were deeply drowned leading to condensed cephalopod limestone reference to the distinctive upper Givetian to accumulation on a former seamount. But middle Frasnian facies at Immouzer-du- during highstands, pelagic anoxic to euxinic

  • Kandar.
  • conditions developed. Upslope, along the

SCHWERMANN (2014): Unspecified record of island shoals, a top Middle to basal Upper shark teeth in Frasnian samples from Devonian reef existed, which was later

  • Immouzer-du-Kandar.
  • uplifted and completely eroded. These strong

RICHTER et al. (2016): Preliminary new contrasts indicate in total a tectonically highly conodont data for the Emsian/Eifelian and active shelf basin slope near to one or more

  • upper Famennian at Immouzer-du-Kandar.
  • islands. After the complex Eovariscan period,

BECKER et al. (2016): Brief reference to the the Viséan strata can be better placed in the discovery of upper Givetian goniatites at palaeogeographic context of adjacent

  • Immouzer-du-Kandar.
  • successions (e.g., BERKHLI et al. 2000).

RICHTER (2017): Unpublished M.Sc. Thesis on the upper Emsian to Eifelian and upper 4. Litho- and biostratigraphy

  • Famennian carbonate succession.
  • Our new studies concentrated on the

TAHIRI et al. (2017): Geochronological dating Emsian to Famennian interval (Fig. 4), but for of granite clasts within the Chabat Jenanet the sake of completeness, earlier and later

  • Conglomerate as Ediacarian and Cambrian.
  • intervals are included and briefly reviewed

COZAR et al. (2019): Discussion of based on literature data. Immouzer-du-Kandar Viséan foraminifers in

the context of survival and/or reworking of 4.1. Silurian-Devonian transition

Lower/Middle Viséan forms into the Upper Viséan.
A thick succession of Pridoli graptolite shales, previously without a formation name (proposal: Douar Rouda Formation), occurs

3. Facies setting and synsedimentary around the Douar Rouda village (WILLEFERT

tectonics et al. 1990, figs. 3-4). At the top, records of

The Immouzer-du-Kandar facies setting Pristiograptus transgrediens and Linograptus

was very complex, with a close superposition posthumus and scyphocrinitid debris give an

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upper Pridoli age. CHARRIÈRE & RÉGNAULT orthoconic cephalopods, nuculid bivalves, (1989) recorded the Lochkovian index and fragmented crinoids. This un-named species Uncinatograptus uniformis from formation may correlate at least partly with several samples but this was not upheld in the the widespread Scyphocrinites Limestone of more detailed study of WILLEFERT et al. the Anti-Atlas (HAUDE et al. 2014) and many (1990). The same applies to a record of other regions (e.g., RÉGNAULT 1985), which “Monograptus hercynicus” (Sample IK 92), straddles the Silurian-Devonian boundary

which was changed to “M.” prognatus.

(e.g., CORRIGA et al. 2013). However, there are no local conodont data so far. Therefore, a lower Lochkovian age still needs to be proven.

4.2. Aïn el Beida Formation (Pragian)

WILLEFERT et al. (1990) illustrated only a faulted lower contact of the thick, fine, rather monotonous, dark-grey, micaceous shales of the Aïn el Beida Formation. It forms a 250 m wide outcrop belt at the SE end of Douar Rouda (BRICE et al. 1984; Fig. 5). The laminated or slightly bioturbated shales yielded, apart from bivalves, gastropods, ostracods, bryozoans, and orthocones, abundant trilobites, including asteropygids, phacopids, and Odontochile (s.l.). The traditional Odontochilinae are most typical for the Pragian and extend into the basal Emsian (e.g., BUDIL et al. 2008). The known brachiopods, crinoids (Asperocrinus), plants (Taeniocrada), acritarchs, and poorly

  • preserved
  • spores

(Camptozonotriletes

caperatus) are not in conflict with a Pragian age (FAIRON-DEMARET & RÉGNAULT 1987). RÉGNAULT & CHAUVEL (1983) discovered a rare stylophorid echinoderm in this formation. The environment was a subtidal, moderately shallow shelf with a constant supply of fine siliciclastics from a hinterland that could have been at some distance. In comparison with the preceding pelagic nodular limestones, the Pragian was locally regressive. But there is currently no record for the middle/upper Lochkovian at Immouzer-du-Kandar (Fig. 3).

Fig. 3: Devonian lithological succession at Immouzerdu-Kandar by FAIRON-DEMARET & RÉGNAULT (1986, fig. 2), with proportions of unit thicknesses and the position of biostratigraphically relevant samples.

The graptolite-rich unit is conformably followed by a thick succession of nodular

  • limestone
  • (“barre
  • noduleuse”)
  • with

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Fig. 4: Revised top-Silurian to Lower Carboniferous lithology and lithostratigraphy at Immouzer-du-Kandar. showing the succession of characteristic fossil groups, facies, seismically triggered reworking episodes, and locally expressed bioevents.

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Fig. 5: Simplified geological cross-section through the Immouzer-du-Kandar Devonian (updated from BRICE et al. 1984, fig. 2, showing their sample numbers = K.-no.; compare more expanded NW-SE cross-section of CHARRIÈRE 1989, fig. 6), using the new lithostratigraphic units.

4.3. Chabat Jenanat Formation (lower which caused gravitational gliding down from

  • Emsian)
  • the original shallow-water setting. Therefore,

The “Poudingue de la Chabat Jenanat” of the local change from subtidal shales and
BRICE et al. (1984) and CHARRIÈRE & siltstones with neritic fauna to coarse RÉGNAULT (1989) is here re-named as Chabat conglomerate and high-turbulence does not Jenanat Formation but restricted to its main necessarily mean a shallowing of the lithology, up to 100 m thick, coarse, strictly environment. It rather reflects a second unsorted and polymict conglomerate with interval of block faulting, which created an well-rounded pebbles (Figs. 5-6; Chabat instable slope.

  • Jenanat Conglomerate). The main lithologies
  • The timing of synsedimentary tectonism

are grey Ordovician quartzites, dark cherts can be deduced from the age of the youngest (perhaps Silurian), slates, Neoproterozoic to observed clast and of the oldest overlying Cambrian granites of unclear regional sediment. Limestone pebbles are very rare but provenance (TAHIRI et al. 2017), and various we extracted one directly from the solid bed acidic volcanites (Figs. 7-8). CHARRIÈRE & that was large enough for microfacies analysis RÉGNAULT (1989) described various tuffs and and conodont dating. It represents a unique, ignimbrites. There is no evidence for any hypoxic, ostracod wackestone (Fig. 9.1) with sorting or grading within thick beds. calcisiltite matrix, a facies type that does not Therefore, sedimentation must have occurred occur in the overlying limestone succession.

  • as violent mass flows in channels along a The
  • single
  • obtained,
  • fragmentary

significant slope. The source for the top- Polygnathus s. str. is too incomplete for Precambrian to Lower Palaeozoic pebbles species identification but its small basal pit is must have been at close distance (within a few a morphological feature that did not develop km). Deep excavation and rounding occurred until the upper half of the lower Emsian (Po. over considerable time in a fluviatile to inversus Zone; e.g., BULTYNCK 1987). Topcoastal setting of an uplifted tectonic block lower to basal upper Emsian conodonts occur forming an island. This enabled the in crinoidal limestones overlying the excavation and mixing of very heterogeneous conglomerate (CYGAN et al. 1990; see below). and heterochronous rocks. Marine re- In consequence, one block tilting phase must sedimentation occurred due to a second phase have occurred within the late lower Emsian, a of seismic activity (see also the sedimentary time interval of ca. 3 ma duration (BECKER et

  • model of CHARRIÈRE & RÉGNAULT 1989),
  • al. 2020 in press). It was capable to uplift

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sediment from subtidal, deeper neritic facies to a coastal level, leading there to rounding and pebble formation. Just slightly later, the pebble was picked up by a seismically triggered mass flow that brought with it much older pebbles that may have been around for a much longer time.
Strong lower Emsian block faulting and reworking is not common in other Meseta regions. BECKER et al. (2015) used the phrase “Eovariscan prelude” for the Lochkovian to Eifelian interval. The closest other evidence for a contemporaneous formation of breccias and olistolite emplacement comes from the Jebel ben Arab between Azrou and Meknes (LAZREQ 1990 and new data). As already noted by CYGAN et al. (1990), it is also no coincidence that the even closer Devonian of Bab-el Ari just NE of Azrou shows a peculiar unconformity high in the lower Emsian, with a subsequent gap encompassing all of the upper Emsian (BOHRMANN & FISCHER 1985). It seems that late lower Emsian tectonism and uplift is a distinctive feature at the NE end of the Western Meseta.

Fig. 6: The coarse, polymict conglomerate (Chabet Jenanat) Formation as exposed at the base of the Jenanat hill.

Fig. 7: Details of the Chabet Jenanat Conglomerate, showing unsorted, well-rounded Lower Palaeozoic (probably Ordovician), light- to middle-grey quartzites and Ediacarian/Cambrian granite (center).

4.4. (new) Chabat Sitout Member (Emsian)

The type area of the new member is at the
Chabet el Sitout valley (BRICE et al. 1984; Fig. 5), ca. 1.5 km SE of the conodont-bearing Section 1 of CYGAN et al. (1990; compare cross-section Unfortunately, succession. in faults complicate
Calcareous shales

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  • Devonian Conodonts in Arizona R

    Devonian Conodonts in Arizona R

    New Mexico Geological Society Downloaded from: http://nmgs.nmt.edu/publications/guidebooks/13 Devonian conodonts in Arizona R. L. Ethington, 1962, pp. 72-76 in: Mogollon Rim Region (East-Central Arizona), Weber, R. H.; Peirce, H. W.; [eds.], New Mexico Geological Society 13th Annual Fall Field Conference Guidebook, 175 p. This is one of many related papers that were included in the 1962 NMGS Fall Field Conference Guidebook. Annual NMGS Fall Field Conference Guidebooks Every fall since 1950, the New Mexico Geological Society (NMGS) has held an annual Fall Field Conference that explores some region of New Mexico (or surrounding states). Always well attended, these conferences provide a guidebook to participants. Besides detailed road logs, the guidebooks contain many well written, edited, and peer-reviewed geoscience papers. These books have set the national standard for geologic guidebooks and are an essential geologic reference for anyone working in or around New Mexico. Free Downloads NMGS has decided to make peer-reviewed papers from our Fall Field Conference guidebooks available for free download. Non-members will have access to guidebook papers two years after publication. Members have access to all papers. This is in keeping with our mission of promoting interest, research, and cooperation regarding geology in New Mexico. However, guidebook sales represent a significant proportion of our operating budget. Therefore, only research papers are available for download. Road logs, mini-papers, maps, stratigraphic charts, and other selected content are available only in the printed guidebooks. Copyright Information Publications of the New Mexico Geological Society, printed and electronic, are protected by the copyright laws of the United States.
  • Size Distribution of the Late Devonian Ammonoid Prolobites: Indication for Possible Mass Spawning Events

    Size Distribution of the Late Devonian Ammonoid Prolobites: Indication for Possible Mass Spawning Events

    Swiss J Geosci (2010) 103:475–494 DOI 10.1007/s00015-010-0036-y Size distribution of the Late Devonian ammonoid Prolobites: indication for possible mass spawning events Sonny Alexander Walton • Dieter Korn • Christian Klug Received: 17 December 2009 / Accepted: 18 October 2010 / Published online: 15 December 2010 Ó Swiss Geological Society 2010 Abstract Worldwide, the ammonoid genus Prolobites is Abbreviations only known from a few localities, and from these fossil SMF Senckenberg Museum, Frankfurt a. M., Germany beds almost all of the specimens are adults as shown by the MB.C. Cephalopod collection of the Museum fu¨r presence of a terminal growth stage. This is in marked Naturkunde Berlin (the collections of Franz contrast to the co-occurring ammonoid genera such as Ademmer, Werner Bottke, and Harald Simon Sporadoceras, Prionoceras, and Platyclymenia. Size dis- are incorporated here) tribution of specimens of Prolobites from three studied localities show that, unlike in the co-occurring ammonoid species, most of the material belongs to adult individuals. The morphometric analysis of Prolobites delphinus Introduction (SANDBERGER &SANDBERGER 1851) demonstrates the intra- specific variability including variants with elliptical coiling The mid-Fammenian (Late Devonian) ammonoid genus and that dimorphism is not detectable. The Prolobites Prolobites is only known from a few localities worldwide, material shows close resemblance to spawning populations mainly in the Rhenish Mountains and the South Urals. of Recent coleoids such as the squid Todarodes filippovae Where it does occur, the majority of the specimens show a ADAM 1975. Possible mass spawning events are discussed terminal growth stage suggesting that these are adults.
  • 284 Conodont Faunal Turnover and Diversity

    284 Conodont Faunal Turnover and Diversity

    284 CONODONT FAUNAL TURNOVER AND DIVERSITY CHANGES THROUGH THE FRASNIAN-FAMENNIAN (F/F) MASS EXTINCTION AND RECOVERY EPISODES MORROW, Jared R., Dept. of Geological Sciences, Univ. of Colorado, Boulder, CO 80309-0250, U.S.A.; SANDBERG, Charles A., Geologist Emeritus, U.S. Geological Survey, Box 25046, MS 940, Federal Center, Denver, CO 80225-0046, U.S.A. Relatively rapid «2 m.y.), stepwise mass extinction during the late Frasnian (mid-Late Devonian) resulted in a major global biomass reduction and loss of up to 82% of tropical marine species. This mass extinction episode culminated at the Frasnian-Famennian (F/F) boundary, which is defined by phyletically-linked species within the conodont genus Palmatolepis. Detailed, computer database-assisted analysis of >50 Euramerican conodont samples from the latest Frasnian linguiformis, and earliest Famennian Early, Middle, and Late triangularis Zones (or chrons of some workers) reveals several steps in the final extinction and subsequent initial recovery of faunas across the boundary. The most marked conodont faunal changes occurred during the 0.3-m.y.-long linguiformis Zone. Diversity and abundance, which were greatest early in the zone, were first significantly reduced within the range ofPalmatolepis linguiformis at the "Upper Kellwasser [deepening] Event" in the middle part of the zone. A second major step took place coincident with an abrupt shallowing event and the apparent extinction of the nominal species late in the zone, following which further steps of diversity-loss occurred. A third, and terrriinal, <0.02-m.y.-long event at the F/F boundary produced the greatest relative extinction. Accompanying these steps were stress-induced increases in short-ranging aberrant and mutant morphotypes within extant species.
  • Pattern and Timing of the Late Devonian Biotic Crisis in Western Canada: Insights from Carbon Isotopes and Astronomical Calibration of Magnetic Susceptibility Data

    Pattern and Timing of the Late Devonian Biotic Crisis in Western Canada: Insights from Carbon Isotopes and Astronomical Calibration of Magnetic Susceptibility Data

    PATTERN AND TIMING OF THE LATE DEVONIAN BIOTIC CRISIS IN WESTERN CANADA: INSIGHTS FROM CARBON ISOTOPES AND ASTRONOMICAL CALIBRATION OF MAGNETIC SUSCEPTIBILITY DATA MICHAEL T. WHALEN Department of Geosciences, University of Alaska, Fairbanks, Alaska 99775-5780 USA e-mail: [email protected] DAVID DE VLEESCHOUWER MARUM–Center for Marine Environmental Sciences, Leobenerstrasse, 28359 Bremen, Germany, and Earth System Sciences, Vrije Universiteit Brussel, Pleinlaan 2, B-1050 Brussels, Belgium JOSHUA H. PAYNE Shell Exploration and Production Co., 150-A North Dairy Ashford, Houston, Texas 77079 USA JAMES E. (JED) DAY Department of Geography–Geology, Illinois State University, Normal, Illinois 61790-4400 USA D. JEFFREY OVER Department of Geological Sciences, State University of New York–Geneseo, Geneseo, New York 14454 USA AND PHILIPPE CLAEYS Earth System Sciences, Vrije Universiteit Brussel, Pleinlaan 2, B-1050 Brussels, Belgium ABSTRACT: Carbon stable isotope data from western Canada, in combination with biostratigraphic control and astrochronologic constraints from magnetic susceptibility data, provide insight into the pace and timing of the Frasnian–Famennian (F–F; Late Devonian) biotic crisis. In much of the world, this event is characterized by two organic-rich shales, which display geochemical anomalies that indicate low-oxygen conditions and carbon burial. These events, commonly referred to as the Lower and Upper Kellwasser events (LKE and UKE), have been linked to the expansion of deeply rooted terrestrial forests and associated changes in soil development, chemical weathering, and Late Devonian climate. The d13C data generated from organic matter record a 3 to 4% positive excursion during each event. These data and other geochemical proxy data reported elsewhere corroborate hypotheses about enhanced biological productivity, driven by terrigenous input under exceptionally warm climatic conditions.
  • Górnodewońskie Goniatyty Gór Œwiętokrzyskich Z Kolekcji Muzeum PIG I Ich Pozycja Stratygraficzna W Skali Konodontowej

    Górnodewońskie Goniatyty Gór Œwiętokrzyskich Z Kolekcji Muzeum PIG I Ich Pozycja Stratygraficzna W Skali Konodontowej

    Przegl¹dGeologiczny,vol.51,nr11,2003 GórnodewoñskiegoniatytyGór ŒwiêtokrzyskichzkolekcjimuzeumPIG iichpozycjastratygraficznawskalikonodontowej TatianaWoroncowa-Marcinowska* Frañskie goniatyty Gór Œwiêtokrzyskich s¹ spotykane 2002), Janczyc (Makowski, 1991), £agów–Dule i okolic sporadycznie i wystêpuj¹ w kilku poziomach.W famenie Galêzic (Sobolew, 1914; Czarnocki, 1989; Wolska, 1967; natomiast znajdujemy je praktycznie we wszystkich pozio- Szulczewski, 1971; Szulczewski i in., 1996). Pozycja stra- mach konodontowych, wy³¹czywszy poziomy górny trian- tygraficzna badanych gatunków podana w podziale g³owo- gularis i dolny/œrodkowy crepida. Kolekcja goniatytów nogowym i konodontowym wed³ug Weddige (1996). zgromadzona przed ponad pó³wieczem w Muzeum Geolo- Frañski zespó³ goniatytów z dolnej czêœci muszlowca gicznym Pañstwowego Instytutu Geologicznego zawiera g³owonogowo-tentakulitoidowego z P³ucek ko³o £agowa okazy zebrane przez J. Czarnockiego, H. Makowskiego i zawiera Archoceras varicosum (Drevermann), Manticoce- M. Ró¿kowsk¹. Obecnie przeprowadzono nie tylko rewi- ras drevermanni Wedekind, M. lamed (G. et F. Sandber- zjê paleontologiczn¹ goniatytów, lecz przebadano tak¿e ger), Crickites neverovi Bogoslovsky, Cr. holzapfeli towarzysz¹ce im konodonty, wydobyte z otaczaj¹cej ska³y. Wedekind, Linguatornoceras aff. clausum (Glenister) oraz Umo¿liwi³o to przypisanie goniatytów okreœlonym pozio- Phoenixites frechi (Wedekind) reprezentuj¹ce poziom mom konodontowym (tab. 1). Crickites holzapfeli i odpowiada poziomowi konodonto- Tabela.1.Pozycjastratygraficznabadanychgatunkówgoniatytówwpodzialekonodontowymig³owonogowym
  • Late Devonian Conodont Fauna of the Gümüflali Formation

    Late Devonian Conodont Fauna of the Gümüflali Formation

    TurkishJournalofEarthSciences (TurkishJ.EarthSci.),Vol.9, 2000,pp.69-89. Copyright©TÜB‹TAK LateDevonianConodontFaunaoftheGümüflali Formation,theEasternTaurides,Turkey fiENOLÇAPKINO⁄LU&‹SMETGED‹K KaradenizTeknikÜniversitesi,JeolojiMühendisli¤iBölümü,TR-61080Trabzon,TURKEY (e-mail:[email protected]) Abstract: TheLateDevonianGümüflaliformationoftheeasternTauridesisaterrigenous-carbonaterocksequence about600mthick,consistingmainlyofquartzsandstone,quartzsiltstone,shale,andcarbonaterocks. Palaeontologicandsedimentologicdatamainlyindicateashallowsubtidaldepositionalenvironment.Thissequence generallyrepresentstheshallow-waterpolygnathid-icriodidbiofacies,andcontainsconodontfaunasthatrange fromtheUpperfalsiovalis ZoneintotheUpperpraesulcata Zone.However,theydonotcorrelatewelltotheLate Devonianstandardconodontzonationbecauseofthelackofzonallydiagnosticspeciesandtheirregularvertical distributionsofthepresenttaxa.Herein,54taxabelongingtoninegeneraaredescribedandillustratedfromthe studiedsection.Icriodusadanaensis,Icriodusfekeensis,andPolygnathusantecompressus arethenewlydescribed species. KeyWords: LateDevonian,conodont,Gümüflaliformation,easternTaurides,Turkey. GümüflaliFormasyonu’nun(Do¤uToroslar,Türkiye)GeçDevoniyen KonodontFaunas› Özet: Do¤uToroslarboyuncayayg›nyüzeylemeleriolanGeçDevoniyenyafll›Gümüflaliformasyonu,yaklafl›k600 metrekal›nl›¤aulaflanbirk›r›nt›l›-karbonatkayadizisidir.Litolojisinibafll›cakuvarskumtafl›,kuvarsmiltafl›,fleylve karbonatkayalar›n›noluflturdu¤ububiriminpaleontolojikvesedimantolojiközellikleri,çökelmeninbafll›cas›¤,gel- gitalt›ortamdageliflti¤ineiflareteder.Konodontfaunas›genelliklek›y›-yak›n›polygnathid-icriodidbiyofasiyesini
  • Conodonts Frorn the Genesee Formation in Western New York

    Conodonts Frorn the Genesee Formation in Western New York

    ·U.S: BUREAu Of MINES P.O. BOX 550 IUNEAU, AlASK} OQ9( ' Conodonts frorn the Genesee Formation in Western New York GEOLOGICAL SURVEY PROFESSIONAL PAPER 1032-B \ Conodonts from the Genesee Formation in Western New York By JOHN W. HUDDLE, assisted by JOHN E. REPETSKI STRATIGRAPHY AND CONODONTS OF THE GENESEE FORMATION (DEVONIAN) IN WESTERN AND CENTRAL NEW YORK GEOLOGICAL SURVEY PROFESSIONAL PAPER 1032-B Conodonts from the Genesee Formatz"on z"n western New York, first descrz"bed by G.]. Hz"nde z"n 1879 and W. L. Bryant z·n 1921, are redescrz"bed, and the b£ostrat£graph£c zones are determz"ned UNITED STATES GOVERNMENT PRINTING OFFICE,WASHINGTON 1981 UNITED STATES DEPARTMENT OF THE INTERIOR JAMES G. WATT, Secreta·ry GEOLOGICAL SURVEY Doyle G. Frederick, Acting Director Library of Congress Cataloging in Publication Data Huddle, John Warfield, 1907-1975 Conodonts from the Genesee Formation in western New York. (Stratigraphy and conodonts of the Genesee Formation (Devonian) in western and central New York) (Geological Survey professional paper ; 1032-B) Bibliography: p. Supt. of Docs. No.: I 19.16:1032-B 1. Conodonts. 2. Paleontology-Devonian. 3. Paleontology-New York (State) I. Title. II. Series. III. Series: United States. Geological Survey. Professional paper ; 1032-B. QE899.H83 557.3'08s [562] 77-608125 For sale by the Distribution Branch, U.S. Geological Survey, 604 South Pickett Street, Alexandria, VA 22304 FOREWORD After John Huddle's death in late November 1975, I was asked to serve as author's representative in the completion of this report. In September 1975, Huddle had completed.
  • Proceedings of the United States National Museum

    Proceedings of the United States National Museum

    A BIBLIOGRAPHY OF THE CONODONTS WITH DE- SCRIPTIONS OF EARLY MISSISSIPPIAN SPECIES By Grace B. Holmes Of the Eastern High School, Washington, D. C. INTRODUCTION The present contributions to the study of the conodonts was pre- pared at the suggestion of Dr. R. S. Bassler and under his direction in the paleontological laboratory of the United States National Museum where extensive collections of these toothlike structures were avail- able. As Doctors Ulrich and Bassler had just completed their paper on the classification of the conodonts and had applied their new classification in the description of an Upper Devonian fauna of western New York and an early Mississippian one from Tennessee, it was thought best that my work should carry these studies to the Mississippian rocks of Alabama and also include for the ready refer- ence by students illustrations of previously described species, with exception of three publications, and a bibliography of the group. The exceptions mentioned refer to the work of Bryant in 1921, Ulrich and Bassler in 1926, and Roundy in 1926, copies of which are still available to the student. ZOOLOGICAL AFFINITIES OF THE CONODONTS The affinities of the conodonts have been a subject of controversy almost since their discovery by Pander in 1856. That there was no doubt in Pander's mind as to their relationship may be ascertained from the title of his monograph. He studied the internal as well as the external structure of the fossils and saw in their formation fishlike characters somewhat of the Selachian type. The question concerning the affinities of these fossils seems to have had its birth in the mind of Dr.