Soil cover and landscape evolution in the Senegal floodplain: a review and synthesis of processes and interactions during the late Holocene

The aim of this paper is to summarize the successive biological, pedological, hydrodynamic, geomorphological and geochemical processes that have occurred in the Senegal valley, and to describe how their interactions during the late Holocene conditioned soil cover formation and landscape evolution. Potential acidity accumulated as pyrite in the floodplain sediment during the last marine transgressions, and was expressed during the following regressions because of oxidation. Soil acidification was mitigated by the soil buffer capacity and by the interaction with the slightly alkaline continental freshwater of the river. Two pedogenetic transformation processes that resulted from the succession of acidic and neutral conditions, transformed unripe muds with pyrite (potential Acid Sulphate soil) to actual Acid Sulphate soils, and then to Vertisols. Geochemical modelling with PHREEQC quantitatively confirmed the feasibility of the processes involved. These two pedogenetic processes also controlled two independent salt accumulation processes: (i) the transformation of shell accumulation beds into gypsum layers and (ii) aeolian deflation and formation of clay dunes. The study shows that pedogenetic effects on alluvial material can lead to contrasting horizons that cannot be explained stratigraphically. It also shows that the presence of saline areas in the Senegal middle valley results from much more complex processes than a simple salt deposition during transgressions.     

Using a structural approach to identify relationships between soil and erosion in a semi-humid forested area, South India

Biogeochemical and hydrological cycles are currently studied on a small experimental forested watershed (4.5 km²) in the semi-humid South India. This paper presents one of the first data referring to the distribution and dynamics of a widespread red soil (Ferralsols and Chromic Luvisols) and black soil (Vertisols and Vertic intergrades) cover, and its possible relationship with the recent development of the erosion process. The soil map was established from the observation of isolated soil profiles and toposequences, and surveys of soil electromagnetic conductivity (EM31, Geonics Ltd), lithology and vegetation. The distribution of the different parts of the soil cover in relation to each other was used to establish the dynamics and chronological order of formation. Results indicate that both topography and lithology (gneiss and amphibolite) have influenced the distribution of the soils. At the downslope, the following parts of the soil covers were distinguished: i) red soil system, ii) black soil system, iii) bleached horizon at the top of the black soil and iv) bleached sandy saprolite at the base of the black soil. The red soil is currently transforming into black soil and the transformation front is moving upslope. In the bottom part of the slope, the chronology appears to be the following: black soil > bleached horizon at the top of the black soil > streambed > bleached horizon below the black soil. It appears that the development of the drainage network is a recent process, which was guided by the presence of thin black soil with a vertic horizon less than 2 m deep. Three distinctive types of erosional landforms have been identified:

1. rotational slips (Type 1);

2. a seepage erosion (Type 2) at the top of the black soil profile;

3. A combination of earthflow and sliding in the non-cohesive saprolite of the gneiss occurs at midslope (Type 3).

Types 1 and 2 erosion are mainly occurring downslope and are always located at the intersection between the streambed and the red soil-black soil contact. Neutron probe monitoring, along an area vulnerable to erosion types 1 and 2, indicates that rotational slips are caused by a temporary watertable at the base of the black soil and within the sandy bleached saprolite, which behaves as a plane of weakness. The watertable is induced by the ephemeral watercourse. Erosion type 2 is caused by seepage of a perched watertable, which occurs after swelling and closing of the cracks of the vertic clay horizon and within a light textured and bleached horizon at the top of black soil.Type 3 erosion is not related to the red soil–black soil system but is caused by the seasonal seepage of saturated throughflow in the sandy saprolite of the gneiss occurring at midslope.     

The effect of resveratrol on the developmental competence of porcine oocytes vitrified at germinal vesicle stage

We tested the effects of resveratrol both as a pre‐treatment and as a recovery treatment after warming during in vitro maturation (IVM) on the viability and developmental competence of porcine oocytes vitrified at the germinal vesicle stage. Pre‐treatment before vitrification of oocytes for 3 hr with 2 μM resveratrol did not affect survival, oocyte maturation and embryo developmental competence to the blastocyst stage after parthenogenetic activation. However, supplementation of the medium with resveratrol during subsequent IVM after vitrification and warming significantly improved the ability of surviving oocytes to develop to the blastocyst stage, and this effect was observed only on vitrified, but not on non‐vitrified oocytes. The intracellular levels of glutathione and hydrogen peroxide in oocytes were not affected by vitrification and resveratrol treatment. Also, there was no significant difference in the occurrence of apoptosis measured by annexin V binding between vitrified and non‐vitrified oocytes, regardless of the resveratrol treatment. In conclusion, resveratrol did not prevent the cellular damages in immature porcine oocytes during vitrification; however, when added to the IVM medium, it specifically improved the developmental competence of vitrified oocytes. Further research will be necessary to clarify the mechanisms of action of resveratrol on the recovery of vitrified oocytes from vitrification‐related damages.