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11. Calpionellids from the Upper Jurassic

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11. Calpionellids from the Upper Jurassic 11. CALPIONELLIDS FROM THE UPPER JURASSIC AND NEOCOMIAN OF DEEP SEA DRILLING PROJECT SITE 416, MOROCCAN BASIN, EASTERN NORTH ATLANTIC Edith Vincent,1 Roger Lehmann,2 William V. Sliter,3 and M. Jean Westberg1 INTRODUCTION From an analysis of variations observed in the struc- ture and compaction of individual turbidite sequences, A "flysch" sequence of Tithonian-Neocomian distal Price (this volume) and Schlager (this volume) conclude turbidites was continuously cored at DSDP Sites 416 that sediment came from two distinct sources to the and 370, in the deep Moroccan Basin, near the foot of east. The first source was offshore carbonate banks, the continental slope, at a water depth of approximately and the second was a detrital province on the continent. 4200 meters (Figure 1). The sites were drilled about 2 km The two sorts of sediments, although arriving separate- apart, during Legs 50 and 41 (Lancelot, Seibold, et al., ly, were often mixed while they were deposited in the ba- 1978) respectively, and their stratigraphic sequences sin by turbidity currents. Hemipelagic, aragonitic lime were combined (Figure 2). muds rich in calpionellids were probably deposited on A detailed lithologic description of the 740-meter the shelf between the carbonate banks and Site 416, and Jurassic-Neocomian section (885-1624 m below sea also on the slope, and were then partly eroded by turbi- floor; Cores 370-35 through 370-51 and Cores 416A-9 dity currents which transported mud pellets and cal- through 416A-57) is given in the Site 416 report (this pionellids to Site 416. volume). This series includes lithologic units VI and Site 416 at the time occupied a very distal position on VII, which consist of alternations of terrigenous and a deep-sea fan system. The sea floor at the site was be- carbonate-rich, thinly bedded cycles (5-20 cm thick) and low the CCD, at a water depth probably well in excess a minor amount of silt-mud laminites and sand layers of 2000 meters, as indicated by arenaceous deep-water with sharp bases and tops. The majority of these cyclic benthic foraminifers (Sliter, this volume). This indig- beds are turbidites, as evidenced by graded bedding, enous foraminifer assemblage occurs only in the upper- erosional bottom structures and easily identifiable, clas- most parts of the turbidite cycles. Other benthic fora- sical Bouma sequences. Unit VII (1430-1624 m; Cores minifers consist of transported and sorted bathyal and 416A-37 through 416A-57) differs from unit VI by the neritic species. common occurrence of hard micritic limestone in the During late Kimmeridgian and Neocomian times, a upper part of the calciturbidite beds and of lithoclasts of widespread regression is recorded in various North At- calpionellid limestone in their coarse basalt parts. The lantic basins. While massive amounts of detrital sedi- calciturbidites of unit VII form a distinct population, ments were poured into the deep Moroccan Basin, ner- with thicker beds than their quartzose equivalents. A itic and littoral sediments were deposited in sedimentary typical calciturbidite consists from bottom to top of (1) basins of southwestern Morocco. Uppermost-Jurassic quartz-bearing calcarenite whose main components are and Berriasian facies in these basins include marly and lithoclasts of micritic limestone (some with calpionel- dolomitic limestones with neritic faunas and floras that lids), skeletal fragments, aptychi, ostracodes, benthic consist largely of calcareous algae and shallow-water foraminifers, and calcisphaerulids; (2) parallel or cross- benthic foraminifers. Calpionellids have been observed laminated, micritic calcisiltite to quartz siltstone, with in the deeper part of the basins, especially in the western skeletal debris, particularly thin shells, and calpionellids Haha Basin (Brun, 1962; Choubert and Faure-Muret, (generally hydrodynamically sorted in layers); (3) dark, 1962; Viotti, 1965; Hottinger, 1966; Société Chérifienne laminated marlstone rich in dolomite(?) rhombs and des Pétroles, 1966). rather well-preserved nannofossils; and (4) laminated, micritic limestone with some marlstone, often burrowed BIOSTRATIGRAPHY AND SEDIMENT from the top. Figures 3 and 4 show examples of varia- ACCUMULATION RATES tions around this ideal sequence. A detailed discussion on vertical variations in indexes of proximity (average From the preceding discussion it appears that all bed thicknesses and percentage of bed containing com- Jurassic-Neocomian calcareous material at Sites 416/ plete or incomplete Bouma sequence) is given in the Site 370 was resedimented from shallower water. Redepo- 416 report (this volume; see also Price, this volume). sition, however, was apparently penecontemporaneous, as indicated by the normal order of first occurrences of species from various fossil groups, making biostrati- graphic zonation possible (Figure 5). Last occurrences 1 Scripps Institution of Oceanography, La Jolla, California 92093. 2 ESSO, EPR-E, 213 Cours Victor-Hugo, 33321 Bègles, France. of species do not appear reliable, as evidenced by com- 3 U. S. Geological Survey, National Center, Reston, Virginia mon upward reworking in all fossil groups. In addi- 22092. tion, the poor preservation of all calcareous microfossils 439 E. VINCENT, R. LEHMANN, W. V. SLITER, M. J. WESTBERG 40°N Agadir Submarine • . Canyon 30°W 25° 20° 15° Figure 1. Location of DSDP Sites 416 and 370. may result in elimination of index species. The possi- There is no direct paleontological evidence of the ex- bility that biostratigraphic boundaries, as placed here, act age of the lowermost sediments reached at Site 416. are stratigraphically too high thus should be kept in However, assuming that Jurassic deposits accumulated mind. The identification of the Jurassic/Cretaceous at the same rate as those of the overlying Berriasian (10 boundary in particular is equivocal, as shown by the m/m.y.), the sediments at the base of the hole would be slight discrepancy between various fossil groups for the of early Tithonian-late Kimmeridgian age, approximate- levels of first occurrence of Berriasian markers. Cal- ly 140 m.y. old. careous nannofossils show the lowest stratigraphic oc- The entire Valanginian-Hauterivian section accumu- currence of Cretaceous species, and nannofossil data lated at the high average rate of 65 m/m.y. No nanno- were utilized here for placement of this boundary (see fossil zonal boundaries could be identified in this se- discussion in Vincent et al., this volume). quence which encompasses the interval from the Cretar- Epoch boundaries based on palynological data are habdus angustiforatus Zone to the Lithraphidites bollii consistently higher in the section than those based on Zone. However, foraminifer datum levels were iden- calcareous nannofossil data, a discrepancy also ob- tified, marking the Valanginian/Hauterivian boundary served at DSDP Site 367 in the Cape Verde Basin to the and possibly the lower/upper Valanginian boundary. south and in wells of the Atlantic continental margin of Although the latter is not clearly marked, there is some North America. Considering the uncertainty in corre- evidence that it occurs near Core 416A-32 (Dorothia lating the palynological zonation with the standard Eu- prehauteriviana, an upper-Valanginian index fossil, oc- ropean stages, palynological data were not taken into curs in and above the latter core, and Trocholina val- account here for age assignment of the Jurassic-Neoco- densis, a lower-Valanginian index fossil occurs below mian sequence (see Vincent et al., this volume). it). Average accumulation rates were estimated using van The highest occurrence of the nannofossil Ru- Hinte's (1976a,b) time scale for age assignments of cinolithus wisei (middle Valanginian) in Core 416A-31 epoch boundaries (Figure 5). However, the poor preser- supports this assumption. It thus appears that the up- vation of faunas and floras and the rarity of biostrati- per-Valanginian section accumulated at a higher aver- graphic data throughout the sequence does not permit a age rate (about 71 m/m.y.) than the underlying lower detailed reconstruction of sedimentation rates. The Valanginian (56 m/m.y.) and the overlying Hauterivian values given in Figure 5 thus represent only average (67 m/m.y.). This inference is in agreement with an in- rates of accumulation for entire intervals, without tak- creased influx of redeposited shallow-water material ing into account either short-term variations within each during that time (Sliter, this volume; see right side of of these intervals or possible hiatuses. Short-term fluc- Figure 5). It is also that interval to which the maximum tuations in accumulation rates probably occurred, in occurrence of calcisphaerulids, which are part of the view of the episodic nature of turbidite sedimentation. calcareous redeposited material, corresponds (Bolli, this The presence of one or more hiatuses is not excluded. volume; Sliter, this volume). For example, it is not clear from nannofossil data The disappearance of micritic limestone beds (mark- whether a hiatus exists between the Berriasian and the ing the top of lithologic unit VII) near the end of the Valanginian (Cepek et al., this volume). Early Valanginian is correlated by Schlager (this vol- 440 CALPIONELLIDS SITES 416 and 370 (Lat. 32 50.2'N; Long. 10 48.TW) cm 95 Nannofossil marl and Nannofossil ooze Turbidites: sandstone, diatom-rich nannofossil marl, and chalk 100 Early Oligocene to Late Eocene Turbidites: mudstone, siltstone, sandstone, gravel, and rare Porcellanite Nannofossil
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