Article number: 23(2):a27
Copyright Paleontological Society, June 2020
Submission: 6 August 2019. Acceptance: 4 June 2020.
The distribution of fossil foraminifera and mollusc assemblages is documented in vibracores recovered from the Namibian and South African shelf to determine changes in depositional environments during the Pleistocene-Holocene. An Uvigerina spp.-dominated assemblage appeared in the early Pleistocene during the intensification of cold-water upwelling of the Benguela Upwelling System (BUS). The palaeoenvironment experienced periodic maximal shoaling after the onset of major glacial periods since the mid-Pleistocene transition (ca. 900 ka) as indicated by the appearance of shallow water benthic foraminifera, dominated by Ammonia japonica and Elphidium spp., replacing Uvigerina spp.-dominated assemblage. The mollusc assemblages also change with Carditella spp., Lucinoma capensis, Nassarius vinctus, Dosinia lupinus, and Tellina analogica becoming the dominant species on the shelf. The benthic foraminifera and molluscs indicate greater productivity over the middle and outer shelf as the BUS intensified and high-amplitude sea-level fluctuations reworked and condensed sediment packages on the shelf. The planktic foraminifera show similarities to other upwelling regions globally, with Globigerina bulloides the dominant species. Warm water species such as Globigerinoides ruber, Globorotalia menardii, and Trilobatus sacculifer occur as minor to trace components attributed to the episodic inflow of warm water currents north and south of the region.
Eugene Bergh. Research Department, Iziko South African Museum, Cape Town 8000, South Africa; Marine Research Institute and Department of Geological Sciences, University of Cape Town, Rondebosch 7701, South Africa.
John Compton. Marine Research Institute and Department of Geological Sciences, University of Cape Town, Rondebosch 7701, South Africa.
Keywords: Pleistocene; Holocene; Namibia; South Africa; Benguela Upwelling System; mid-Pleistocene transition; sea level
Final citation: Bergh, Eugene W. and Compton, John S. 2020. Quaternary foraminifera and mollusc assemblages on the southwestern African shelf. Palaeontologia Electronica, 23(2):a27. https://doi.org/10.26879/1018
Copyright: June 2020 Paleontological Society.
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The sediments underlying the Benguela Upwelling System (BUS) are enriched in organic carbon (Pedersen and Calvert, 1990; Shannon and Nelson, 1996; Mollenhauer et al., 2002), with sediment deposition on the continental margin during the Pleistocene being influenced by high-amplitude sea-level fluctuations during glacial-interglacial cycles (Diester-Haass et al., 1992; Mollenhauer et al., 2002; Compton and Wiltshire, 2009). Namibian shelf sediments are phosphorite-rich (Compton and Bergh, 2016), and the high productivity of the system has contributed to a high abundance of fossils (foraminifera, molluscs, ostracods, fish remains) on the continental shelf, which is important in palaeoenvironmental and geologic studies. How the microfossil and fossil (mainly molluscs) assemblages on the Namibian shelf have been influenced by Pleistocene sea-level fluctuations has previously not been investigated and can provide a biostratigraphic reference to one of the world’s most productive upwelling regions focused over the shelf. Previous studies on surface grab samples (Martin, 1974, 1981; Lowry, 1987; Giraudeau, 1993; Schmidt-Sinns, 2008) focussed on the occurrences of species around the Namibian and South African coast, but, because limited to surface samples, did not allow for palaeoceanographic reconstructions of the BUS. Exploration for phosphorite deposits on the shelf has provided a large number of vibracores and owing to the highly condensed deposits, these cores provide, for the first time, a stratigraphic record from the Neogene to Recent.
Much of the research on the Pleistocene history of the BUS has focused on slope sediments along the southwestern margin of Africa owing to Deep Sea Drilling Program (DSDP) Leg 75, sites 362, 530-532 (Hay et al., 1984), and Ocean Drilling Program (ODP) Leg 175, sites 1080 to 1087 (Wefer et al., 1998). The cores retrieved from these expeditions allowed for the interpretation of palaeoceanographic and assemblage changes over time. These slope sediments have been studied to determine sediment deposition (Diester-Haass and Rothe, 1987; Robinson et al., 2002), upwelling intensity (Baumann and Freitag, 2004) and productivity (Schmiedl and Mackensen, 1997; Marlow et al., 2000; Rau et al., 2002; Jahn et al., 2003; Baumann and Freitag, 2004; Lazarus et al., 2008) along the southwestern continental margin of southern Africa.
Foraminifera from cores and sediments from the western continental shelf of southern Africa allow for the biostratigraphy and interpretation of palaeoenvironments along the shelf. South African shelf foraminifera have provided information on the stratigraphy of sediments and their associated palaeoenvironments from the Miocene to Holocene (Dale and McMillan, 1999; Compton et al., 2002, 2004; Franceschini and Compton, 2004). More recent work involving foraminifera on the Namibian shelf included the occurrence of foraminifera in anoxic environments along the Namibian margin (Leiter and Altenbach, 2010) and the biostratigraphy of shelf sediments (Compton and Bergh, 2016; Bergh et al., 2018). Compton and Bergh (2016) provided detailed analyses on the stratigraphy, formation, and geochemistry of the phosphorite deposits on the Namibian shelf and included species lists of foraminifera and molluscs to support the strontium isotope stratigraphy and age model of the sediments.
Using new data from the Namibian continental shelf and previous studies from the western South African shelf, this paper aims to identify Quaternary foraminiferal and molluscan assemblages to document how they relate to Pleistocene sea-level fluctuations. In particular, these assemblages provide a record of palaeoenvironmental shifts, such as substrate, bathymetry, and bottom water conditions associated with changes in sea level, corresponding to the intensification of the BUS during the Quaternary. The biostratigraphy and palaeoenvironmental reconstructions are important in phosphorite exploration and in documenting how taxa respond to long-term palaeoceanographic changes in a major coastal upwelling region.
GEOLOGIC AND OCEANOGRAPHIC SETTING
The study area is situated offshore between Walvis Bay and Lüderitz on the central Namibian continental shelf to the northern Namibian continental shelf, south of the Kunene River mouth (Figure 1). The Namibian margin formed during the rifting of Gondwana during the Cretaceous period. The continental shelf extends to 400 m and is divided into an inner (0 to 130 m), middle (130 to 200 m), and outer shelf (200 to 500 m) (Rogers, 1977). The Walvis Ridge extends from the northern Namibian continental margin to the Mid-Atlantic Ridge to the west and acts as a barrier to deep-water flow (Berger et al., 1998).
Precambrian basement rocks are exposed on the rocky shoreline and inner shelf. Neogene and Quaternary sediments unconformably overlay Cretaceous and early Cenozoic strata (Bremner, 1977). Neogene sediments and strata on the shelf are condensed as a result of non-deposition, erosion, eustatic sea level lowering, episodic tectonic uplift, and the intensification of aridity in the continental interior (Dingle et al., 1983; Wigley and Compton, 2006; Bergh et al., 2018). Relict phosphorite deposits are exposed on the middle to outer shelf between 130 and 400 m water depth (Compton and Bergh, 2016). The 2 m condensed Pliocene-Pleistocene phosphorite-rich deposits on the shelf are contrasted by nannofossil and diatomaceous mud deposits 400-600 m thick (Meyers et al., 1998) on the upper slope (Compton and Bergh, 2016). A diatomaceous mud belt dated to the Holocene extends from south of the Kunene River mouth to Walvis Bay and is largely confined to the inner shelf (Bremner, 1977).
The BUS along the Namibian margin is highly productive with cold, upwelled, nutrient-rich waters influencing sedimentation along the continental shelf (Lutjeharms and Stockton, 1987). The colder waters of the BUS are influenced by subpolar deep water masses and upwelled by southeast trade winds that blow alongshore (Shannon and Nelson, 1996).The Benguela Current (BC) forms the eastern limb of the South Atlantic gyre and is distinct from the BUS. The cold upwelled waters of the BC are bounded by warmer currents to the north and south. To the north, the BC meets the warmer Angola Current at the Angola-Benguela Front (ABF) (Moroshkin et al., 1970) and to the south the BC meets the Agulhas Current, which originates in the warmer Indian Ocean. The Agulhas Current flows westwards south of South Africa before it retroflects back eastwards south of the BUS. Some of the warmer waters from the Agulhas Current can flow into the BUS, transporting warmer water foraminifera taxa into the area (Rau et al., 2002).
MATERIALS AND METHODS
Twenty vibracores less than 2 m in length from the continental shelf between the Walvis Bay-Lüderitz (16 cores) and northern Namibian shelf (4 cores) (Figure 1) were retrieved by Minemakers Pty. Ltd. in 2008 and 2012, respectively. The cores were selected based on stratigraphic and faunal lists documented in Compton and Bergh (2016). The cores were logged and split into working and archive halves. The Walvis Bay-Lüderitz cores consist of two clusters, namely the Conception and Meob Bay clusters (Figure 1). The cores were sampled along depth intervals where contacts were clear and every 10 to 20 cm where units were greater than 10 cm thick. Samples selected at contacts allowed for environmental changes to be tested for during different time intervals. The samples were washed, sieved, and split into <63 μm (mud), 63 μm to 2 mm (sand) and >2 mm (gravel) fractions. The sand fractions were put in an ultrasonic cleaner for up to 1 minute to ensure all particles were disaggregated. Five cores, based on the completeness of their stratigraphy and length of record, were selected from the shallow middle (core 1307 - 199 m; core 1441 - 223 m), shallow outer (core 1401 - 244 m; core 1479 - 245 m), and deep outer shelf (core 1406 - 309 m).
Foraminifera (from the separated sand fractions) and molluscs (from the separated gravel fractions) were identified in all 20 cores. Foraminifera, other biogenic and mineral (detrital and authigenic) components in the five selected cores were counted under a stereomicroscope to at least 300 individuals per sample to determine the dominant taxa (highest relative abundance) on which palaeoenvironmental interpretations rely. Foraminifera were counted in representative splits if individuals accounted for more than 300 in the samples. Where foraminifera were less abundant, all individuals were counted in the entire sample. The mean relative abundances of the biogenic and mineral components, reported as percentages, were calculated from these counts.
Whole mollusc shells and fragments were counted to determine the relative abundances. Intact bivalve shells, and where complete shells were present and matched another shell, were counted as one individual. Complete intact bivalve shells and complete gastropod shells may give an indication of minimal transport. Fragments were identified based on a part of a shell that is broken or where multiple fragments were present. Only fragments that could be attributed to certain species were assigned to that species.
The core lithology is presented in Compton and Bergh (2016) and reveals an overall coarsening upward succession (Figure 2). Cores 1405, 1408, and 1406 consist of a basal olive-green mud unit grading into coarser sandy units with biogenic and authigenic grains towards the top of the cores. Six units were identified in the Walvis Bay-Lüderitz cores (Compton and Bergh, 2016). Units 6 and 5 are olive green mud units with abundant fragmented foraminifera dated to the Pliocene. Unit 4 is a black to leached brown pelletal phosphorite sandy unit (Figure 3). Unit 3 is a slightly shelly sandy unit, whereas unit 2 is a shelly sandy unit that contains abundant shell material and whole shells. Gravel components (large bone fragments, phosphorite pebbles and concretionary phosphorite nodules) result in units 5 to 2 having coarser grain sizes in some cores. Unit 1 is a sandy gravel unit containing abundant shell fragments, whole mollusc shells and foraminifera.
Representative microfossils were picked for scanning electron microscope (SEM) imaging. The microfossils were mounted onto black adhesive carbon tabs and coated with a thin layer of Gold-Palladium using a BIO-RAD SEM coating system before SEM images were taken with a JEOL JSM-5200 scanning microscope at Iziko Museums in Cape Town.
The age model for the cores was based on a combination of strontium isotope stratigraphy (SIS) and biostragraphic planktic foraminiferal indicator species (Compton and Bergh, 2016; Bergh et al., 2018). The different sand and gravel components (foraminifera, pelletal phosphorite grains, concretionary phosphorite pebbles, fragmented fish bones, teeth, scales, and mollusc shell fragments) were previously picked from bulk gravel and sand-sized material and run for strontium isotope analysis (Compton and Bergh, 2016). Planktic foraminiferal indicator species were identified based on Kennett and Srinivasan (1983) and Bolli et al. (1985).
Statistical analyses were performed using the PAlaeontologicalSTatistics (PAST) data analysis package (Hammer et al., 2001). Hierarchical cluster analysis was used to estimate similarities in species composition in samples to determine sub-assemblages within the core stratigraphy with Ward’s method and Euclidean distance applied.
Stratigraphy and Sedimentology
The sediment of the olive-green muds contains abundant foraminifera (55-98%) with minor amounts of echinoid spines, shell fragments, fish bone material, ostracods, and pelletal phosphorite in intercalated lenses towards the top of the base unit.
With the exception of the mud unit, the pelletal phosphorite content decreases up-core (Figure 3) with a maximum abundance (mean of 88.5%) in the sandy units (unit 4). Shell contents are highest (mean = 12.3%) in the shelly gravel unit (unit 1). Foraminifera are most abundant (mean = 85.4%) in the sand fractions of the olive-green mud unit (unit 5). Above unit 4 the foraminiferal abundance increases upwards and reaches a mean abundance of 12.3% in unit 1.
Bone material in the sand fractions comprises a small amount and only attains its highest abundance (mean = 5.8%) in the sandy units (unit 4). Other components remain negligible (<1%) throughout the successions of the cores and include echinoid spines, fish otoliths, sponge spicules, ostracods, and bryozoan fragments.
The most abundant planktic foraminiferal species preserved in all the units is Globigerina bulloides (min. = 46.9%; max. = 100%) decreasing in abundance (Figure 4) towards the less shelly units. The maximum percentage of G. bulloides preserved in the sediments was encountered in one sample of unit 3 in core 1479. Planktic species Globorotalia (Globoconella) inflata and Globigerinoides ruber (white) (<2%) have higher abundances in unit 3 relative to units 2 and 1, whereas Neogloboquadrina incompta recorded similar abundances across all the units with the highest abundance in unit 3. Other planktic species with low relative abundances (<1%) in both the central Namibian and northern Namibian shelf include Neogloboquadrina dutertrei and Globigerinella siphonifera. Orbulina universa recorded low numbers (<1%) on the central Namibian shelf, but higher relative abundances on the northern Namibian shelf (<47%).
The pelletal phosphorite sandy unit 4 with more than 80% pelletal phosphorite sand content generally does not contain foraminifera (Figure 3). Very few foraminifera in the sediments are agglutinated (<1% abundance) and miliolids accounted for <1% of the foraminiferal assemblages in the shelly sandy units. The classification of biofacies on foraminiferal assemblages corresponds to sedimentological units of the cores.
Unit 3 recorded higher proportions of Uvigerina peregrina with Cassidulina laevigata and Bolivina spathulata (syn. Brizalina spathulata) increasing towards the contact between units 3 and 2. Unit 2 still had abundant Uvigerina spp. but their relative abundances decreased towards the contact between units 2 and 1, and B. spathulata maintained similar abundances (Figure 5). Unit 2 also recorded higher Elphidium advenum abundances. Unit 1 is characterised by the dominance of Ammonia japonica and higher relative E. advenum abundances.
The dominant species in the upper units of the cores (unit 1 in Walvis Bay-Lüderitz) are A. japonica and Elphidium spp. with Cassidulina laevigata recording similar relative abundances between the two areas. Relative abundances for Cibicidoides lobatulus (syn. Lobatula lobatula) are higher (>10%) in the less gravelly units of the northern Namibian cores south of the Kunene River mouth compared to cores in the Walvis Bay-Lüderitz area. In the less gravelly units of the northern cores, Nonion boueanus recorded abundances of >40%. In the deepest core south of the Kunene River mouth occurrences of Globobulimina turgida reach relative abundances >50%.
Cluster analysis divided the units containing abundant Uvigerina spp., B. Spathulata, and A. japonica into three main fossil assemblages based on their relative abundances. These assemblages are (1) Uvigerina spp., (2) Uvigerina spp.-A. japonica-B. Spathulata, and (3) A. japonica (Figure 6).
The 25 analysed samples from the five selected cores yielded a total of 86 whole or near-whole bivalve shells and 110 gastropod shells, which could be assigned to 13 bivalve taxonomic groups (genus and species level) and five gastropod taxonomic groups (genus and species level). The upper portions of the northern Namibian as well as the Walvis Bay-Lüderitz cores reveal similar dominant mollusc species. The most abundant whole bivalve shells are Carditella sp. and Lucinoma capensis in unit 2 of the Walvis Bay-Lüderitz cores (Figure 7-Figure 8). Lucinoma capensis is the most abundant fragmented shell. The dominant gastropod species throughout all the cores are Nassarius vinctus in whole and fragmented forms with Turritella declivis only observed in unit 2. Marginella spp. are observed in both units of the Walvis Bay-Lüderitz cores. In unit 2, Dosinia lupinus and Tellina analogica form a minor component (<10%) in whole and fragmented forms, but increase in relative abundance to become dominant species in unit 1. The bivalve species Carditella sp. and Nucula nucleus mostly occur as whole shells while Lucinoma capensis mostly occurs as fragments in unit 1.
The bivalve Pecten spp. was the only species (in fragmented form; Figure 9) to have been observed in the olive-green mud unit of the northern Namibian cores. The dominant gastropod in the overlying gravelly sandy phosphorite units of the northern Namibian cores is Nassarius vinctus (Figure 10) throughout, with Volutacorbis lutosa and Comitas saldanhae present, but in lower numbers. The dominant bivalve species in the layers below the upper 10 cm of the northern Namibian cores are Lucinoma capensis and Tellina analogica (whole and fragmented). The bivalve species Dosinia lupinus, Carditella sp., and Nuculana bicuspidata are among the major bivalve components as whole shells, but decrease in the fragmented fraction. In the upper 10 cm of the cores Dosinia lupinus and Tellina analogica are the dominant bivalves in whole shell form, whereas specimens of Lucinoma capensis are more abundant in the fragmented fraction.
The most abundant planktic foraminiferal species preserved at the middle to outer shelf depths along the Namibian shelf during the Quaternary are G. bulloides and Gr. (Gc.) inflata (Figure 11). Low abundances of Gs. ruber were recorded for the northern Namibian shelf and the Walvis Bay-Lüderitz region. Along the northern Namibian shelf Ng. incompta (previously Ng. pachyderma dextral) also occurs in relatively high abundances, specifically in the less shelly units. Previous studies from onshore deposits (Dale and McMillan, 1999; McMillan, 1990a, 1990b) reported few to no planktic tests where Pleistocene environments were shallower than the outer shelf deposits (<300 m). This marks a progression of increased species diversity and abundances from shallow water inner to middle shelf environments preserved in onshore highstand deposits to the outer shelf and slope.
Many of the benthic foraminiferal species recorded in this study have wide distributions stretching from the northern Namibian shelf to the south and east coasts of South Africa. These taxa are commonly associated with cosmopolitan species (Lowry, 1987; and references therein). Two samples collected by Schmiedl (1995) at water depths of 173 m (GeoB 1021, southern Angolan shelf) and 250 m (GeoB 1013, central Angolan shelf) reveal assemblages with similar taxa. The benthic species Bulimina marginata, Cassidulina laevigata, Lobatula lobatula, Globobulimina turgida, and Uvigerina peregrina were recorded at both sites by Schmiedl (1995), while Bulimina gibba and Elphidium advenum were found to occur only at the shallower site. Schmidt-Sinns (2008) also found the distribution of taxa on the inner shelf to be widespread between Cape Town and southern Angola. The species Quinqueloculina seminula, Rectuvigerina nicoli, Bulimina elongata, Bulimina gibba, Cancris auriculus, Cassidulina laevigata, Uvigerina peregrina, and Elphidium advenum recorded in this study were also found by Schmidt-Sinns (2008) to occur at inner shelf depths (Figure 12, Figure 13, Figure 14).
Foraminifera recorded in surface grab sediments (Lowry, 1987) have also been recorded in Pleistocene sediments and outcrops (Dale and McMillan, 1999; Compton et al., 2002, 2004; Franceschini and Compton, 2004; Compton and Bergh, 2016; this study) and on the Holocene mud belt of South Africa (Dale and McMillan, 1998). McMillan (1990a) recorded similar benthic taxa from borehole and outcrop samples of the Upper Algoa Group along the south coast of South Africa which include Ammonia spp., Elphidium spp., Nonion boueanus, Cibicidoides lobatulus, Quinqueloculina cf. seminula, Cancris auriculus, Bulimina gibba, and Brizalina spathulata.
Most of the foraminifera species on the outer shelf occurring in Pleistocene, Holocene, and surface grab samples first appeared in the sediment record during the Pliocene-Pleistocene transition. These assemblages are generally absent in older deposits, corresponding with the timing of the period in which the BUS intensified along the margin. Franceschini and Compton (2004), however, dated first occurrences of Cibicidoides lobatulus, Ammonia spp. and Elphidium crispum from shallow water environments to the late Miocene/Pliocene using SIS. This is in contrast to outer shelf deposits of Namibia as the Miocene-Pliocene assemblages contain deeper water species (Bergh et al., 2018) and do not record similar species observed in the onshore South African marine deposits as noted by Franceschini and Compton (2004). These species may have existed at inner shelf water depths not sampled in this study.
The major taxa between the Namibian shelf and the South African western shelf (Compton et al., 2004) are similar with minor species and diversity changes likely attributed to small-scale ecosystem heterogeneities linked to substrate, seasonality, and periodicity of coastal upwelling, in addition to differences in organic matter fluxes and dissolved oxygen contents in bottom waters (Schmiedl et al., 1997). For example, Schmidt-Sinns (2008) found bottom water dissolved oxygen to be the major driver behind the differences between faunal compositions of the Southern Benguela and Northern Benguela regions.
Foraminifera on the Namibian Shelf Compared to Slope Foraminifera
The three major planktic species recorded in this study, G. bulloides, Gr. (Gc.) inflata and Ng. incompta, are also the dominant species recorded along the upper slope (Wefer et al., 1998) (Table 1) and continue to be the dominant species today (Giraudeau, 1993). Modern distributions of G. bulloides show higher relative abundances along the shelf of Namibia whereas Gr. (Gc.) inflata increases towards the slope off northern Namibia and western South Africa. Higher relative abundances of Ng. incompta also occur along the Namibian margin (Giraudeau, 1993).
Pleistocene foraminifera along the Namibian continental shelf are distinct from those along the slope (Figure 15). Present-day foraminifera on the slope are also distinct from outer shelf foraminifera (below 400 m on the broad continental shelf of southwestern Africa) and are strongly influenced by the Oxygen Minimum Zone (OMZ) and related biogeochemical gradients (Schmiedl et al., 1997). The dominant slope species during the late Pleistocene off Namibia were Bulimina spp. and Uvigerina hispidocostata. Shelf species are largely absent in slope sediments. Trace to minor abundances (<1 to 10%) of A. japonica and Hyalinea balthica were reported for the Plio-Pleistocene along the slope of Namibia and western South Africa (Wefer et al., 1998). On the northern Namibian slope very low abundances (generally <1%) of Quinqueloculina spp. were reported for the Pleistocene (Berger et al., 1998). Relative abundances of Quinqueloculina seminula were also found to be very low (<1%) in this study area. The other species present in slope sediments that are also present in Pleistocene shelf sediments is Cassidulina laevigata, but this species has a broader bathymetric range and has been documented to occur at slope depths (Schmiedl et al., 1997). Cassidulina laevigata is a minor component of the slope assemblages during the early Pliocene becoming a major component during the late Pliocene and Pleistocene. Slope sediments also indicate Bulimina marginata to be a minor component (<10% relative abundance) of the assemblages along Namibia and South Africa during the Plio-Pleistocene.
The differences in shelf and slope assemblages, as well as the differences in sediment composition, imply that very few foraminiferal tests and other sand-sized grains are transported from the shelf to the slope. The flow velocities of most bottom currents observed along the margin are too weak to suspend coarser sandy material from the shelf to the slope (Shannon and Nelson, 1996) and will winnow away muddy sediment and leave sand-sized material, including foraminifera on the shelf. Bottom currents are stronger during glacial sea-level lowstands. Compton and Wiltshire (2009) noted the transport and deposition of quartz and glauconite grains from the outermost shelf to the slope of western South Africa during glacial lowstands. The fluctuating strength of the internal tides, bottom currents, turbidity flows (from rare seismic activity) and flow velocities during the Pleistocene thus account for the transport and deposition of the few shelf species documented in slope sediments in minor to trace amounts.
Foraminifera and Molluscs Indicate Cooling, Shoaling, and Increased Productivity along the Margin
Subtropical sea surface conditions indicated by warm water species Gs. ruber, T. Sacculifer, and T. immaturus during the middle Miocene (Bergh et al., 2018) cooled during the Pliocene-Pleistocene transition when G. bulloides and Gr. (Gc.) inflata became the dominant planktic taxa. Abundant G. bulloides has been recorded in upper Pliocene sediments along the northeastern margin of South America, also associated with upwelling and cooling (Ibaraki, 1997). The Pliocene sediments off Walvis Bay-Lüderitz contain a mixture of deep benthic and warm subtropical planktic foraminifera. Together with G. bulloides and Gr. (Gc.) inflata the Pliocene foraminifera indicate changing conditions associated with the initiation of the BUS during the Miocene/Pliocene along the Namibian margin (Compton and Bergh, 2016). The faunal turnover is also consistent with cooling periods between 3 and 2 Ma and 1.5 to 0.5 Ma when Namibian sea surface temperatures (SST) decreased by 3 to 5°C (Marlow et al., 2000; Lazarus et al., 2006; Etourneau et al., 2009). Marlow et al. (2000) recorded a 10°C decline in sea surface temperatures (SST) since 3.2 Ma linked to global cooling and increased upwelling associated with strengthening of southeasterly trade winds (Shi et al., 2001) along the margin.
The Angola-Benguela Front is characterised by Gr. (Gc.) inflata-G. bulloides (Ufkes et al., 1998) and similar assemblages, especially regarding the presence and abundance of G. bulloides. The dominant taxa between these assemblages are the same, but the relative abundances of these taxa and minor taxa vary. Studies with deeper water environments off Central and West Africa (e.g. Ufkes et al., 1998) record a higher number of taxa, but the assemblages also contain the same minor species (Ga. siphonifera, Gs. ruber, Gs. sacculifer, Gr. menardii, Gr. truncatulinoides, Ng. dutertrei, Ng, pachyderma, Ng. incompta, and O. universa) recorded in this study. Relatively high abundances of G. bulloides have been reported from other major upwelling regions as well, such as the Arabian Sea (Prell and Curry, 1981; Curry et al., 1992; Peeters et al., 2002), northwest Africa (Martinez et al., 1999), the eastern margin of South America (Ibaraki, 1997; Marchant et al., 1999; Mohtadi et al., 2005) and California (Sautter and Thunell, 1991). Gr. (Gc.) inflata and G. bulloides are regarded as transitional species (Kucera, 2007), and high relative abundances of G. bulloides are also an indicator of strong upwelling conditions (Giraudeau, 1993).
The abundance of warm subtropical to tropical Gs. ruber decreases (Figure 4) during the Pleistocene along the Namibian shelf and Globorotalia menardii and T. sacculifer are low in numbers. These warm water species with minor abundances reach the Benguela Region through the inflow of warmer waters from the Angola Current to the north (Kemle-von Mücke and Oberhänsli, 1999) and the transport of low salinity, tropical waters into the Southern Benguela Region from the Agulhas Current (Rau et al., 2002). The high abundance of Orbulina universa, identified as a subtropical species by Kucera (2007), on the northern Namibian shelf during the Pleistocene indicates the influence and proximity of the Angola Current to the north.
The Namibian outer shelf cores indicate Miocene-Pliocene benthic foraminifera (Bergh et al., 2018) being replaced by an Uvigerina spp.-dominated assemblage during the Pliocene-Pleistocene transition (Compton and Bergh, 2016). The localised faunal turnover during the Pliocene-Pleistocene corresponds with intensification of the BUS (Compton and Bergh, 2016) and the onset of major Northern Hemisphere glaciation, climate cooling and increased glacial cycle amplitudes (Lisiecki and Raymo, 2007).
The three assemblages identified in the Pleistocene units correspond with the three stratigraphic units dated to the early, mid, and late Pleistocene (Figure 6). These changes in assemblage indicate changes in palaeoceanographic conditions, including upwelling intensity, bottom water oxygen and bathymetry related to large sea-level fluctuations, particularly after the mid-Pleistocene transition circa 900 ka.
Infaunal foraminifera such as Uvigerina spp. became the dominant taxa in the early Pleistocene when bottom water conditions became more suitable for foraminifera adapted to more eutrophic and dysoxic conditions along the northern Namibian shelf, whereas suboxic indicators were more dominant during the Miocene-Pliocene (Bergh et al., 2018). The benthic species Uvigerina peregrina has been described as a shallow infaunal species adapted to relatively high amounts of organic matter input under variable oxygenated bottom waters more adapted to dysoxic conditions (Fontanier et al., 2002; Koho et al., 2008). Environments with mostly infaunal foraminifera and low diversities are characteristic of eutrophic conditions. Benthic faunal compositions are dependent upon oxygenation and organic detritus, i.e., food supply reaching the ocean floor (e.g., Altenbach and Sarnthein, 1989; Jorissen et al., 1995; Fariduddin and Loubere, 1997; Jorissen et al., 1998). The high relative abundances of Uvigerina spp. are consistent with the occurrences of this taxon in reported eutrophic environments under high organic carbon fluxes typical of upwelling regions such as the BUS (Fontanier et al., 2002; Licari and Mackensen, 2005).
In eutrophic environments the vertical distribution of foraminifera is more dependent on oxygen availability where oxygen concentrations fall below the lower limits of epifaunal taxa. Only deep infaunal taxa adapted to dysoxic conditions will survive below this limit as opposed to oligotrophic environments where more oxygen is consumed at the epifaunal-shallow infaunal level (Jorissen et al., 1995). The results from the Walvis Bay-Lüderitz cores are in agreement with findings by Bergh et al. (2018), which found that the benthic environment changed from oligotrophic conditions prior to the onset of the BUS in the late Miocene to eutrophic conditions after BUS initiation along the northern Namibian shelf.
Epifaunal abundances increased during the middle Pleistocene (Figure 16). The Mid-Pleistocene Transition (MPT) marks the change in climatic cycles where global ice volume variations shift from being controlled by 41 kyr to 100 kyr cycles (Hays et al., 1976; Pisias and Moore, 1981; Imbrie et al., 1992; Raymo and Nisancioglu, 2003; Elderfield et al., 2012). Sea-level amplitudes increased during the middle Pleistocene dropping by as much as 125 m (Miller et al., 2005). The study area was closer to the shoreline during sea level lowstands and shallow-water foraminifera (A. japonica and E. advenum) increased in abundance (Figure 17), which accounts for the observed infaunal-epifaunal ratios found in this study. These taxa indicate estuarine and littoral conditions as evidenced by previous work on foraminifera from the western shelf (McMillan, 1990b; Dale and McMillan, 1998; Dale and McMillan, 1999; Compton et al., 2002, 2004; Franceschini and Compton, 2004; Franceschini et al., 2005; Franceschini and Compton, 2007; Herbert and Compton, 2007) and south coast sediments of South Africa (McMillan, 1990a). The increasing abundance of epifaunal foraminifera along the shelf of Namibia and western South Africa is indicative of environments where a more diverse range of microhabitats are available, e.g., hard and rocky substrates for these foraminifera to attach mixed with softer substrate to burrow into. These shallow water foraminifera were close enough to where the outer shelf is today to be transported into the deeper area during lowered sea levels of glacial maxima (Compton and Wiltshire, 2009).
A comparison between the onshore deposits (Dale and McMillan, 1999) and saltwater marsh foraminifera from southwestern South Africa (Franceschini and Compton, 2004; Franceschini et al., 2005; Franceschini and Compton, 2007) and the outer shelf foraminifera from western South Africa (Compton et al., 2002, 2004) indicate that taxa associated with littoral environments are preserved in onshore deposits and taxa associated with inner shelf environments are preserved in outer shelf sediments off western South Africa. This is consistent with data from this study in which inner shelf species are preserved in outer shelf sediments of Namibia.
The mollusc assemblages across the Namibian shelf indicate similar shallow marine environments. The most abundant mollusc species in unit 2 of the Walvis Bay-Lüderitz cores, Lucinoma capensis, Turritella declivis, and Comitas saldanhae, occur where B. spathulata and Uvigerina spp. show higher abundances. The dominance of Lucinoma capensis in the shelly sandy units signal organic-rich conditions at the sea floor in the center of upwelling cells (Edelman-Fürstenberg, 2014) and Turritella declivis has been associated with upwelling conditions (Allman, 1988). The occurrence of Turritella declivis indicates water depths of 40 to 220 m based on present-day occurrences of the species along the south coast of South Africa. Substrate indications based on T. declivis are however broad, as they can occur in thick mud to coarse gravelly sands (Herbert, 2013).
The distribution of molluscs in the BUS (Table 2) is influenced by substrate, oxygen content, upwelling conditions, microhabitats, and depth (Edelman-Fürstenberg, 2014; and references therein). Marine transgressions during the late Pleistocene created numerous lagoons, estuaries, and embayments along the coast (Tankard and Rogers, 1978). This accounts for the variability in the mollusc assemblages accumulating in the outer shelf deposits of Namibia and South Africa. During the late Pleistocene to Holocene Dosinia lupinus replaced Lucinoma capensis as the dominant bivalve species being preserved in the sediments. During the Holocene off southwest South Africa the dominant bivalve species was also Dosinia lupinus, while Nassarius vinctus and Volutocorbis lutosa are the dominant gastropod species (Compton et al., 2002; Herbert and Compton, 2007). The present-day fauna on the shelf is still composed of abundant Dosinia lupinus (Barnard, 1964; Kilburn and Rippey, 1982). The dominance of the infaunal filter-feeding species Lucinoma capensis and Dosinia lupinus indicates fine grained sedimentation on the shelf (Barnard, 1964; Kensley, 1978; Kilburn and Rippey, 1982), and the turnover of abundant species Dosinia lupinus in unit 1 supports a shoaling marginal marine environment (Edelman-Fürstenberg, 2014) of up to 150 m (Walker et al., 2000), a water depth consistent with the dominance of Ammonia spp. Similar to shallow water foraminifera, Dosinia lupinus is associated with estuarine influences and environments (Branch et al., 2007). Namibian perennial rivers are rare but estuarine influences in the study area could be associated with the Kuiseb River south of Walvis Bay (Watson and Lemon, 1985; Bate, 1993; Meadows, 2001) and the Kunene River (Wearne and Underhill, 2005). Prodelta to delta front sandy and muddy conditions are indicated by the occurrence of the gastropod species Nassarius vinctus in unit 1 at water depths of less than 100 m when the sea level was up to 125 m below present-day during the Last Glacial Maximum (LGM) (Miller et al., 2005). The good preservation of the shells, and in places articulated valves, indicate minimal disturbance, consistent with lowered sea level during the LGM and the accumulation of abundant Dosinia valves in the uppermost unit of the cores. Alternatively, the autochthonous deposition of articulated valves could also be explained during sea level rise, descending wave and current energy and rapid sediment burial which would cause minimal disturbance, as shown for example in the Orange River prodelta (Compton et al., 2002).
Upwelling indicator species and transitional planktic species along the Namibian margin appear in Pliocene-Pleistocene sediments, which are associated with the initiation of the BUS during the late Miocene to Pliocene. The present-day assemblages and foraminifera on the shelf in surface grab samples from previous studies can be traced back in vibracores from the shelf to the Pleistocene during a period in which the BUS intensified. The major planktic species is interpreted to be controlled by the cold upwelled waters. The planktic foraminifera are dominated by transitional to cold water species with minor occurrences of warm water species Globigerinoides ruber, Globorotalia menardii, Trilobatus sacculifer, and Orbulina universa. The minor occurrences of warm water species are attributed to the inflow of warm currents from the north (Angola Current) and south (Agulhas Current) of the BUS and the high abundances of Orbulina universa on the northern Namibian shelf to the proximity of the Angola Current.
The wide distribution of the major benthic foraminiferal taxa stretching across the BUS and into the south and east coasts of South Africa are controlled by the microhabitat which, in turn, is influenced by substrate, organic matter fluxes and dissolved bottom water oxygen contents. Only a few species, such as Hyalinea balthica, Quinqueloculina seminula, Cassidulina laevigata, and Bulimina marginata recorded from the outer shelf are recorded in trace to minor amounts on the slope. Apart from some taxa, such as Cassidulina spp. and Bulimina spp., having broad bathymetric ranges, there is minimal transport from the shelf to slope as energy dispersion is too weak and the shelf too broad to suspend and transport sand-sized components, such as foraminifera.
A palaeoenvironmental shift from relatively deep to shallow depths is recorded in Pleistocene sediments along the southwestern shelf of southern Africa. The Miocene-Pliocene to Pliocene-Pleistocene marks a period in which oceanographic and climate changes led to the turnover of foraminiferal assemblages along the southwestern margin of Africa from a warm subtropical assemblage to colder, shallow water assemblages. The shift in the palaeo-environment during the Pleistocene was most noticeable in the Walvis Bay-Lüderitz region where outer shelf sediments reveal an Uvigerina spp.-dominated assemblage in the lower Pleistocene. The Uvigerina spp.-assemblage indicates eutrophic conditions under high organic carbon conditions. During the MPT, Uvigerina spp. relative abundances decrease and epifaunal foraminifera increase indicating slightly less eutrophic conditions. This assemblage occurs together with the mollusc species Lucinoma capensis, Turritella declivis, and Comitas saldanhae, which indicate increased upwelling conditions. During the upper Pleistocene an Ammonia japonica-assemblage is established and the dominance of the Lucinoma capensis bivalve species replaced by Dosinia lupinus indicating mostly taxa adapted to suboxic conditions with increased epifaunal abundances in marginal marine to inner shelf environments.
The upper Pleistocene to Holocene foraminifera and molluscs are recorded in a wide range of depositional settings along the shelf of southern Africa, which include the outer shelf, the mudbelt on the inner shelf, estuarine, lagoonal and beach environments. Their high relative abundance in the uppermost sections of the cores indicates a strong influence of estuarine, lagoonal and beach environments on the middle to outer shelf sediments.
The foraminifera and mollusc assemblages indicate that the palaeoenvironment of the area was shoaling during the Pleistocene, especially when compared to the Miocene-Pliocene assemblages, and is consistent with higher amplitude sea-level fluctuations, particularly sea-level lowstands of as much as 125 m below present sea level after the Mid-Pleistocene Transition. The water depth thus lowered from a deep outer shelf environment in the middle Miocene to early Pliocene to palaeodepths fluctuating between the inner and middle shelf during the Pleistocene.
Comments and suggestions to the manuscript were provided by P. Frenzel, G. Schmiedl, M. Kaminski, M. Kucera, H. Filipsson, and an anonymous reviewer. The cores were provided by Minemakers Pty. Ltd. Melissa Oosthuizen assisted in the laboratory with processing of some of the Northern Namibian core material.
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