Geological setting of Pliocene rifting and deposition in the Afar Depression of Ethiopia

Tectonic extension of the Afar amounts to 10–30 km since 1–2 Ma and to 40–60 km since 3–5 Ma ago, or rougly 1–2 cm per year. Active faulting, volcanism, and development of the Pliocene and younger Afar grabens with their rich hominid and other vertebratefaunas, have been controlled by ENE and WNW oriented lineaments or ancient zones of structural weakness. These lineaments also controlled the alignment of the Gulf of Aden and Red Sea, respectively.Crustal stresses resulting from the late Miocene (Messinian) salinity crisis in the Mediterranean basin may have triggered renewed tectonic movements along certain pre-existing lineaments such as the Levant Shear. Separation of Africa from Arabia (and hence the inception of Afar) was controlled by tectonic events far removed from NE Africa, including possible Miocene fusion of the Indo-Arabian plates.During the early Pliocene, the Ethiopian uplands were far lower (possibly by 1000 m) and the southern Afar-Middle Awash region was higher, so that topographic and climatic contrasts between plain and plateau were less pronounced and the Afar climate was less arid than today.There was a major change from lacustrine to fluviatile deposition in the Middle Awash valley soon after 4·0–3·8 Ma ago, caused by extensional tectonics. Within the topographic constraints imposed by volcano-tectonic activity, regional climatic oscillations have controlled the detailed pattern of Pliocene (and later) sedimentation in Afar.     

Temperature compensation in the mammalian cell cycle

Random and synchronous V79 cells were shifted from 37.5 °C to temperatures between 29 ° and 41 °C. Intermitotic time determinations of random cultures showed an increase in generation time and a broadening in the distribution of generation times in cells whose cycle spanned the temperature shift, but only a slight increase in generation time after one generation at temperatures between 34 °–40 °C. At 33.5 °C and below there was a stepwise increase in generation time. When cells grown at non-standard temperatures were allowed to habituate for 48 h at the altered temperature prior to analysis, the increase in median intermitotic time was slightly less in comparison to analyses done after only one generation following the temperature step. The Q₁₀ for cell division of cells growing at temperatures from 34 ° to 40 °C was between 1.15 and 1.26, suggesting that the mammalian cell cycle is temperature compensated over a limited (6–7 °C) temperature span. Mammalian cells in culture appear to have the same capacity for temperature compensation in their cell cycle as do unicellular eukaryotes. The fact that cycle time at lower temperatures increases in a discrete manner is taken as evidence for a quantal clock.     

Evidence for acyl chain trans/gauche isomerization during the thermal pretransition of dipalmitoyl phosphatidylcholine bilayer dispersions

In order to clarify, in dipalmitoyl phosphatidylcholine multilayers, the effect of the 34°C thermal pretransition on the acyl chain intramolecular disordering process, Raman spectra of dipalmitoyl phosphatidylcholine gels at 20 and 34°C were compared in the 1000–1200 cm⁻¹ skeletal C-C stretching region. In addition to an overall intensity decrease associated with a change in chain packing characteristics, the growth of intensity in the 1080–1090 and 1122 cm⁻¹ regions in the (34-20°C) difference spectrum clearly indicates that the thermal pretransition is accompanied by an increase in the population of hydrocarbon chain gauche rotamers toward the center of the bilayer.     

Lacustrine sedimentation in the diapir-controlled Miocene Bicorb Basin, eastern Spain

The Miocene Bicorb Basin is a small elongated basin developed by normal faulting of a thick Jurassic–Cretaceous carbonate succession and subsequent diapirism of Upper Triassic mudstones and evaporites. The basin fill comprises a sequence over 650 m thick formed by two units. The lower, alluvial unit consists of a complex alternation of conglomerates, sandstones, mudstones, and minor lacustrine limestones. The upper unit comprises marginal alluvial and lacustrine deposits in which seven lacustrine facies associations have been distinguished. The inner lacustrine deposits comprise mudstones and carbonates with minor evaporitic deposits. At the northeast and southwest basin edges, alluvial inputs led to the development of delta and fan-delta environments where sandstone and conglomerate deposits dominate. The latter stages of the lake evolution are represented by an expansive thick limestone sequence which close to the NW fault-bounded margin pass laterally to breccias. The hierarchical arrangement of the upper unit shows five different orders of sequences. The first-order sequence defines a major vertical trend of lake expansion whereas three second-order sequences are linked to major flooding-expansion episodes. All these sequences are related to the tectonic evolution of the diapir. Metre-scale, third- and fourth-order sequences and fifth-order sequences, which consist of finely laminated rhythmite deposits probably record climatically forced processes. The diapir–graben system evolution and the climatic variations have exerted major controls on the sequential arrangement and evolution of the lacustrine system. Both factors have also strongly influenced the changes in the gastropod assemblages.     

Water permeation through the lipid bilayer membrane. Test of the liquid hydrocarbon model

According to the liquid hydrocarbon model, the lipid bilayer is viewed simply as a thin slice of bulk hydrocarbon liquid. This allows the water permeability of the bilayer to be calculated from bulk properties. In this paper the prediction of the liquid hydrocarbon model is compared with the known water permeability coefficient of the glycerol monoolein/n-hexadecane bilayer (Fettiplace, R. (1978) Biochim. Biophys. Acta 513, 1–10). As the alkyl chain of glycerol monoolein is equivalent to 8-heptadecene, the water permeability coefficient of 8-heptadecene/n-hexadecane mixtures was measured for temperatures between 20 and 35°C. The mole fraction of n-hexadecane in the bulk liquid was chosen at each temperature to match the known mole fraction of n-hexadecane in the bilayer (White, S. (1976) Nature 262, 421–422). The predicted water permeability coefficient agrees with the measured value at 32°C but is 40% above the measured value at 20°C. The apparent activation energy predicted by the liquid hydrocarbon model is 9.0 ± 0.3 kcal/mol, while the measured value is 14.2 ± 1.0 kcal/mol. The failure of the liquid hydrocarbon model probably results from a different molecular organization of the hydrocarbon chains in the bilayer and in the bulk liquid.     

Formation of extracellular and intracellular ice during warming of vitrified mouse morulae and its effect on embryo survival

In vitrified solutions, ice can form during warming if the concentration of the cryoprotectant is insufficient. For the cryopreservation of cells, ice is innocuous when it remains outside the cell, but intracellular ice (ICI) is lethal. We tried to estimate the conditions in which ICI forms in vitrified mouse morulae during warming. The solutions for the experiments (EFS10–EFS50) contained 10–50% ethylene glycol plus Ficoll plus sucrose. When vitrified EFS20, EFS30, and EFS40 were kept at −80 °C, they remained transparent after 3 min, but turned opaque after 60 min (EFS20, EFS30) or 24 h (EFS40). Morulae were vitrified with EFS solutions after exposure for 30–120 s at 25 °C. They were warmed by various methods and survival was assessed in culture. After rapid warming (control), survival was high with EFS30 (79–93%) and EFS40 (96–99%). After slow warming, survival decreased with both EFS30 (48–62%) and EFS40 (44–64%). This must be from the formation of ICI. To examine the temperature at which ICI formed during slow warming, vitrified embryos were kept at various sub-zero temperatures during warming. Survival with EFS30 and EFS40 decreased on keeping samples for 3 min at −80 (25–75%), −60 (7–49%), −40 (0–41%), or −20 °C (26–60%). When samples were kept at −80 °C for 24 h, the survival decreased to 0–14%. These results suggest that ICI forms at a wide range of temperatures including −80 and −20 °C, more likely between −60 and −40 °C, and the ice forms not only quickly but also slowly.     

Turkana Basin-Middle Awash Valley correlations and the age of the Sagantole and Hadar Formations

The Moiti, Lomogol and Wargolo Tuffs of the Turkana Basin correlate with similar layers in the Sagantole Formation exposed in the Middle Awash Valley, Ethiopia. These correlations demonstrate that the tephrostratigraphy of the Turkana Basin can be applied to the Middle Awash Valley. Consideration of our analyses together with previous analyses shows that more volcanic ash layers are present in the Sagantole Formation than have been reported and also that the proposed correlation of VT-2 between Bodo and Belohdelie is incorrect. In addition, the correlations suggest that the age of the Cindery Tuff of the Sagntole Formation is about 3·8 Ma, at the young end of the range proposed earlier (3·8–4·0 Ma). This implies that the hominid skull fragments from the Sagantole Formation are 3·8–3·9 Ma. The upper part of the Sagantole Formation contains the Lomogol Tuff (ca. 3·6 Ma). Because the Sagantole Formation underlies the Hadar Formation, the base of the Hadar Formation can be no older than 3·8 Ma and is probably younger than 3·6 Ma, in agreement with correlation of the Tulu Bor (ca. 3·35 Ma) and Sidi Hakoma Tuffs. As all hominid fossils presently known from the Hadar Formation are younger than the Sidi Hakoma Tuff, they must be younger than 3·35 Ma. This estimate agrees with faunal evidence from the lower part of the Hadar Formation, and allows placement of hominids from Laetoli, the Middle Awash Valley and the Turkana Basin in temporal order.     

Trace fossils and rhizoliths as a tool for sedimentological and palaeoenvironmental analysis of ancient continental evaporite successions

Recognition of evaporite formations from continental Tertiary basins of Spain provides evidence that trace fossils (including rhizoliths) can be abundant in some saline lake systems and their study helps in palaeoenvironmental interpretation of ancient continental evaporite sequences. Six main types of trace fossils have been distinguished and include: (1) networks of small rhizoliths; (2) large rhizoliths; (3) tangle-patterned small burrows; (4) isolated large burrows; (5) L-shaped traces; and (6) vertebrate tracks. Rhizoliths were related to both marginal areas of hypersaline lakes and lakes of moderately high saline waters. In these settings, pedoturbation resulted from colonization by grasses and bushes of distinct lake subenvironments. The activity of burrowing invertebrate faunas was especially intense in lakes of moderately concentrated brines from which gypsum was the main evaporite mineral deposited. A specific gypsum lithofacies (‘bioturbated gypsum deposits') forming thick, massive beds has a widespread occurrence in many of the basins. Tangle-patterned small burrows and minor isolated large burrows constitute the typical trace fossil types within the gypsum. The traces are interpreted as having been caused by burrowing insect larvae, probably chironomids, coleopterans and annelids. The behaviour of these organisms in recent lake environments yields information about the salinity range of lake waters from which gypsum precipitated. Concentration values averaging 100–150 g/l may be thus deduced though some organisms involved in the formation of the traces can tolerate higher salinities. The combined analysis of lithofacies and trace fossils from the lacustrine evaporite sequences contributes to the study of distinct saline lake subenvironments as well as changes in the sedimentary evolution of the lake systems. Consequently, trace fossils can provide valuable insight for palaeoenvironmental analysis of at least some evaporite formations that accumulated in continental settings.     

Late Quaternary stratigraphy and sedimentology of Orphan Basin: Implications for meltwater dispersal in the southern Labrador Sea

Orphan Basin is a deep-water basin on the continental margin off Newfoundland, which throughout the late Quaternary received proglacial sediment from local ice that crossed the continental shelf. Sediment from more distant sources was transported southward in the Labrador Current as proglacial plumes and in icebergs. Five sedimentary facies related to glacial processes are distinguished in cores recovered from Orphan Basin: hemipelagic sediment, nepheloid-layer deposits (layered mud), beds rich in ice-rafted detritus (IRD), sand and mud turbidites, and glaciogenic debris-flow deposits. IRD-rich beds correspond to periods of intensified iceberg calving, and layered mud, turbidites, and glaciogenic debris-flow deposits with glacial meltwater discharge.

In the Late Wisconsinan, eight periods of meltwater discharge and iceberg calving from the Newfoundland ice sheet are interpreted from the sediment facies in Orphan Basin. These discharges coincide with the terminations of the colder periods of the D–O cycles recorded in Greenland ice cores. The oldest minor meltwater event (27.5–28.5 cal ka) corresponds to the first Late Wisconsinan ice advance across the Grand Banks and NE Newfoundland Shelf. The following three meltwater discharges (23–23.5, 23.8–24.5, and 25–27 cal ka) deposited sand turbidites and glaciogenic debris-flow deposits seaward of Trinity Trough, which was occupied by an ice stream at this time, and mud turbidites in the southern part of the basin derived from a mid-shelf ice margin on the Grand Banks. Four periods of meltwater discharge occurred during the deglaciation and are centered at 15, 18.5, 19.75, and 20.75 cal ka. The youngest is correlated to Heinrich event 1. In the literature, the 18.5 and 20.75 cal ka events have been recorded in multiple glacial settings in the North Atlantic, and therefore, are interpreted as large-scale events of meltwater discharge and iceberg calving, but in Orphan Basin the 19.75 cal ka event is also of similar scale.     

Tectonic and sedimentary evolution of basins in the northeast of Qinghai-Tibet Plateau and their implication for the northward growth of the Plateau

The northeast of the Qinghai-Tibet Plateau, from the Hoh Xil Basin to the Hexi Corridor Basin, demonstrates a basin-ridge geomorphy that is the result of the long-term uplift of the Qinghai-Tibet Plateau. The geological evolution of the Qinghai-Tibet Plateau is recorded in its associated basins. From the Cenozoic sedimentary filling pattern in the Hoh Xil, Qaidam and Jiuquan Basins, we find that the evolution of these basins is similar: they began as strike-slip basins, evolved into foreland basins, and then to intermontane basins. Foreland basins are the direct result of orogenic activity in the northeast of Qinghai-Tibet Plateau, and can be documented to have formed over the following time periods: 49-23 Ma for the Hoh Xil foreland basin, 46-2.45 Ma for the Qaidam foreland basin, and 29.5-0 Ma for the Jiuquan foreland basin. This northward migration in the timing of foreland basin development suggests that the northeastern part of Tibet grew at least in part by accretion of Cenozoic sedimentary basins to its northern margin.     

The effect of calcium on temperature-induced phase changes in liquid-crystalline cardiolipin structure

The temperature-dependent fluidity of lamellar and Ca²⁺-precipitated cardiolipin structures was investigated over the temperature range 5–55 °C, using the stearic acid spin labels I(12.3), I(5.10), and I(1.14). In the lamellar phase the I(12.3) label reflects an abrupt thermotropic change of the membrane fluidity at 37 °C. The I(5.10) and I(1.14) labels show two points of phase changes located at 14, 36 °C and 10, 38 °C, respectively. The Ca²⁺-complexed cardiolipin structures provoke a retraction of the hydrocarbon chains, preferentially in the polar region, and at the same time a loss of the phase transitions.     

Trace fossil analysis of lacustrine facies and basins

Two ichnofacies are typical of lacustrine depositional systems. The Scoyenia ichnofacies characterizes transitional terrestrial/nonmarine aquatic substrates, periodically inundated or desiccated, and therefore is commonly present in lake margin facies. The Mermia ichnofacies is associated with well oxygenated, permanent subaqueous, fine-grained substrates of hydrologically open, perennial lakes. Bathymetric zonations within the Mermia ichnofacies are complicated by the wide variability of lacustrine systems. Detected proximal–distal trends are useful within particular lake basins, but commonly difficult to extrapolate to other lakes. Other potential ichnofacies include the typically marine Skolithos ichnofacies for high-energy zones of lakes and substrate-controlled, still unnamed ichnofacies, associated to lake margin deposits. Trace fossils are useful for sedimentologic analysis of event beds. Lacustrine turbidites are characterized by low-diversity suites, reflecting colonization by opportunistic organisms after the turbidite event. Underflow current beds record animal activity contemporaneous with nearly continuous sedimentation. Ichnologic studies may also help to distinguish between marine and lacustrine turbidites. Deep-marine turbidites host the Nereites ichnofacies that consists of high diversity of ornate grazing traces and graphoglyptids, recording highly specialized feeding strategies developed to solve the problem of the scarcity of food in the deep sea. Deep lacustrine environments contain the Mermia ichnofacies, which is dominated by unspecialized grazing and feeding traces probably related to the abundance and accessibility of food in lacustrine systems. The lower diversity of lacustrine ichnofaunas in comparison with deep-sea assemblages more likely reflects lower species diversity as a consequence of less stable conditions. Increase of depth and extent of bioturbation through geologic time produced a clear signature in the ichnofabric record of lacustrine facies. Paleozoic lacustrine ichnofaunas are typically dominated by surface trails with little associated bioturbation. During the Mesozoic, bioturbation depth was higher in lake margin facies than in fully lacustrine deposits. While significant degrees of bioturbation were attained in lake margin facies during the Triassic, major biogenic disruption of primary bedding in subaqueous lacustrine deposits did not occur until the Cretaceous.     

Comparison of an aquatic invertebrate assemblage between an old-growth natural forest and planted coniferous forest basins in a Japanese temperate region: the Kuroson stream in the Shimanto River basin

The purpose of this study is to clarify the differences in the aquatic invertebrate assemblage between the two basins that have the most common types of Japanese headstream forests – an old-growth natural forest (ONF) and a planted coniferous forest (PCF) – in the Kuroson stream of the Shimanto River basin and to find the groups that tend to inhabit either the ONF basin or PCF basin. Abundance, the number of families and -diversity were not different between the two basins. However, a cluster analysis of similarity showed differences in aquatic invertebrate assemblages between the ONF and PCF basins and that this difference was brought about by specific characteristics of some families, such as the Taeniopterygidae and Athericidae. We suggest that differences in the aquatic invertebrate assemblages between the two basins are a reflection of differences in the composition of the forest vegetation.     

A Late Triassic lake system in East Greenland: facies, depositional cycles and palaeoclimate

The Upper Triassic Fleming Fjord Formation of the Jameson Land Basin in East Greenland contains a well-exposed succession, 200–300 m thick, of lake deposits. The Malmros Klint Member, 100–130 m thick, is composed of cyclically bedded intraformational conglomerates, red siltstones and fine-grained sandstones and disrupted dolomitic sediments (paleosols). The cyclicity is composite with cycles having mean thicknesses of (25), 5.9 and 1.6 m. The overlying Carlsberg Fjord beds of the Ørsted Dal Member, 80–115 m thick, are composed of structureless red mudstones rhythmically broken by thin greyish siltstones. This unit also has a composite cyclicity with cycles having mean thicknesses of 5.0 and 1.0 m. The uppermost Tait Bjerg Beds of the Ørsted Dal Member, 50–65 m thick, can be divided into two units. A lower unit is composed of cyclically bedded intraformational conglomerates or thin sandstones, red mudstones, greenish mudstones and yellowish marlstones. An upper unit is composed of relatively simple cycles of grey mudstones and yellowish marlstones. Recognized cycles have mean thicknesses of 5.6 and 1.6 m. The lake deposits contain evidence of seasonal, orbital and long-term climatic change. Seasonal change is documented by numerous desiccation surfaces especially in the Malmros Klint Member and Carlsberg Fjord beds, orbital change is suggested by the composite cyclicity, and long-term climatic change is indicated by the systematic upwards change in sedimentary characteristics of the lake deposits. The sedimentary features of the Malmros Klint Member suggest lacustrine deposition in a dry climate that fluctuated between desert and steppe conditions, the Carlsberg Fjord beds probably record lacustrine lake deposition in a rather constant dry (steppe) climate, while the Tait Bjerg Beds record lake sedimentation in a climate that fluctuated between dry (steppe) and warm moist temperate. In the Tait Bjerg Beds the upward change in cycle characteristics indicates a shift towards more humid conditions. Climatic deductions from sedimentary facies are in good agreement with climate maps of Laurasia, as simulated by numerical climate models. Palaeomagnetic data indicate a northward drift of East Greenland of about 10° from ca. 25°N to ca. 35°N in the Middle to Late Triassic. The Fleming Fjord Formation which represents ca. 5 m.y. of the Late Triassic interval was deposited during latitudinal drift of 1–2°. It is possible that the observed long-term upward shift in climatic indicators within the formation can be ascribed to plate drift, but southward shift of climatic belts could also have been of importance.     

Using species-specific paleotemperature equations with foraminifera: a case study in the Southern California Bight

Species-specific paleotemperature equations were used to reconstruct a record of temperature from foraminiferal δ¹⁸O values over the last 25 kyr in the Southern California Bight. The equations yield similar temperatures for the δ¹⁸O values of Globigerina bulloides and Neogloboquadrina pachyderma. In contrast, applying a single paleotemperature equation to G. bulloides and N. pachyderma δ¹⁸O yields different temperatures, which has been used to suggest that these species record the surface-to-thermocline temperature gradient. In Santa Barbara Basin, an isotopically distinct morphotype of G. bulloides dominates during glacial intervals and yields temperatures that appear too cold when using a paleotemperature equation calibrated for the morphotype common today. When a more appropriate paleotemperature equation is used for glacial G. bulloides, we obtain more realistic glacial temperatures. Glacial–interglacial temperature differences (G–I ΔT) calculated in the present study indicate significant cooling (8–10°C) throughout the Southern California Bight during the last glacial maximum (LGM). The magnitude of glacial cooling varies from 8°C near the middle of the Southern California Bight (Tanner Basin and San Nicolas Basin) to 9°C in the north (Santa Barbara Basin) and 9.5–10°C in the south (Velero Basin and No Name Basin). Our temperature calculations agree well with previous estimates based on the modern analog technique. In contrast, studies using N. pachyderma coiling ratios, U^k′₃₇ indices, and transfer functions estimate considerably warmer LGM temperatures and smaller G–I ΔT.     

Thermostable α-amylase from derepressed Bacillus licheniformis produced in high yields from glucose

High yields of thermostable α-amylase was produced by Bacillus licheniformis 44MB82-G, resistant to glucose catabolite repression, on the basis of inexpensive raw materials and glucose as a main carbon source. The optimal parameters for the α-amylase production were an agitation rate of 500 rpm, constant air-flow rate (1 vvm) and cultivation temperature 40°C. An enzyme activity of 4800–5000 U/ml culture medium was reached in 96–120 h. The α-amylase preparation had the following characteristics: α-amylase activity 55 000 U/ml, high thermostability (98% residual α-amylase activity after 10 min treatment at 90°C), protein content 88 mg/ml and dry substances 30%.     

Rainbow trout (Oncorhynchus mykiss) recombinant IL-1β and derived peptides induce migration of head-kidney leucocytes in vitro

The present work provides the first information concerning the chemoattractant activity of trout recombinant IL-1β and its derived peptides, referred to as P1, P2 and P3. The predicted rainbow trout mature interleukin-1β peptide was produced as a recombinant protein in Escherichia coli. The first peptide, P1, corresponded to fragment 146–157 (YVTPVPIETEAR) of the trout sequence and had an MW of 1·37 kDa. It was equivalent to a region known to be part of the receptor binding domain from the mammalian crystal structure of IL-1β complexed to its receptor. P2 was used as control peptide, consisting of the same 12 amino acids as P1, but arranged in a random sequence (VVEEYIRAPPTT). P3 was synthesised to complex with an adjacent region of the IL-1 receptor, and corresponded to fragment 207–216 (YRRNTGVDIS) of the trout sequence, with an MW of 1·18 kDa. Migration was stimulated when leucocytes were exposed to concentrations of ≥10 ng ml⁻¹rIL-1β. Peptide P3 also induced leucocyte migration, with an optimal dose of 0·25 mm being recorded. While P1 had no effect on cell migration when used alone, synergism was evident as a consequence of combining P1 with a suboptimal dose (0·01 mm) of P3. No synergism occurred when cells were exposed to a combination of P3 and the control peptide P2.     

Late Albian dinoflagellate cyst paleobiogeography as indicator of asymmetric sea surface temperature gradient on both hemispheres with southern high latitudes warmer than northern ones

Late Albian temperature sensitive dinoflagellate cysts are characterized in order to better understand mid-Cretaceous sea surface temperature gradients. Distribution maps of thirty-seven species recovered from one hundred fifty outcrops and deep sea drilling holes (ODP, DSDP) Sites located from low and high paleolatitudes over the two hemispheres (75°N–70°S) are encountered. Fifty years of published data available in eighty-seven articles have been considered and synthesized using a database coupled with a Geographical Information System (GIS). The continuous and disjoint biogeographic patterns of dinocyst species along latitudes define seven climatic belts, four in the northern hemisphere (high, mid-high, mid-low, low latitude belts) and three in the southern hemisphere (low, mid-low, mid-high latitude belts). Dinocysts restricted along latitudes are temperature sensitive species. Limit ranges of temperature sensitive dinocysts of mid-low and mid-high latitude belts reveal mixing belts, located at 40–45°N and 50°–70°S. They represent major palaeofrontal systems as paleosubtropical fronts with strongly mixed water column. The northern frontal system (40–45°N) was located as in the modern ocean. The large southern frontal system (50°S–70°S) was 10°–20° poleward to Antarctica. Semi-quantitative temperature range limits for mid-Cretaceous dinoflagellates and SST gradients in the two hemispheres are suggested by setting dinocyst climatic belts against estimated δ¹⁸O temperature curve from fish teeth. A paleoecological classification is suggested. Latitudinal distribution of extant temperature sensitive dinoflagellate cysts follows the asymmetric modern temperature gradient. Asymmetric latitudinal ranges of Late Albian dinocyst species of mid-low latitude belts restricted between 45°N and 70°S demonstrate asymmetric temperature gradients with southern high latitudes being warmer than northern high latitudes.     

Tectonic and volcanic controls on Early Jurassic rift-valley lake deposition during emplacement of Karoo flood basalts, southern Namibia

The Karoo Igneous Province of southern Africa is one of the classic Mesozoic flood basalt provinces of the world. In the case of the early Jurassic Kalkrand Formation of Namibia the succession comprises three major flood basalt units that are separated by two stratigraphically important fluvio-lacustrine interlayers. These horizons preserve a record of the complex interplay between sedimentation, effusion of Karoo flood basalts and extensional tectonics that predated and accompanied the break-up of Gondwanaland. Both sediment layers start with the dominantly local derivation of weathered and eroded lava debris, followed by the emplacement of subaqueous mass flows and subsequent deposition of chemical sediments. The latter are characterised by interbedded stromatolitic carbonates, grass-like structured gypsum, and plane-bedded sandstones and mudstones containing euhedral displacive gypsum crystals that grew in the subsurface as well as rosettes which nucleated on the sediment surface. The central parts of the lacustrine units are overlain by thin deltaic sandstones showing bottomset, foreset, and topset layering and, finally, braided fluvial, trough cross-bedded sandstones. Evidence of subsidence synchronous with the formation of lake bodies can be explained by two principal mechanisms. The first acted in localised areas only and is reflected by the development of small, centrally subsiding basins. From the repeated occurrence of onlapping geometries within such a pool, a multiphase history of sagging is deduced, being most likely related to periodic magma withdrawal and reduction in magmatic pressures in subsurface lava feeders beneath the basin floor. Abundant syn-subsident fracture features at lava–sediment contacts, such as sediment-, hydrothermal calcite-, and sometimes basic lava-filled fissure systems indicate the pronounced interaction between the underlying volcanics and these small areas of pronounced subsidence. Fluids passing through the volcanic pile exhaled into the lake, giving it the characteristics of alkaline lake systems described from more recent flood basalt areas associated with the modern African Rift System. On the regional scale, however, northerly trending extensional fault systems controlled half-graben basin geometries and both facies and thickness variations across faults indicate that tectonism operated contemporaneously with volcanism and lacustrine sedimentation. The analysis of faults and associated structures, such as regularly aligned sediment-filled fissures, sets of micro-faults, folds and basaltic dykes constrains the extensional opening direction for the Karoo graben structures in this area that heralded the opening of the South Atlantic and thus provides a basis to discuss the extensional history of the Namibian coastal margin within the regional tectonic framework.