This thesis provides a comprehensive application of a source-to-sink approach for terrestrial organic material delivered by riverine transport to the mudbelt offshore South Africa and was based on a solely terrestrially produced biomarker. The comparison of the origin of terrestrial organic and inorganic material clearly indicates that the source of the used proxy has to be known before interpreting marine archives. The suspension loads and the flood deposits reflect a similar overprinting of local plant contribution during the riverine transport. However, suspension loads and flood deposits only represent “snapshots” of the transported signal. Therefore, it is recommended to investigate the plant wax signal with respect to different seasons to detect potentially differences of the transported signal between rainy and non-rainy seasons. The implications of additional terrestrial input from the adjacent west coast biomes (Fynbos and Succulent Karoo) should be further tested. It remains unclear how much terrestrial material is transported either by wind or by riverine transport from this region. Studies considering the aeolian input have shown that the wind driven transport may be negligible south of the Orange River mouth (Prospero et al., 2002; Dupont and Wyputta, 2003; Eckardt and Kuring, 2005; Vickery et al., 2013), while the ephemeral rivers along the west coast contribute sediment to the mudbelt only during flood conditions. Parallel investigations of dust samples and suspension
6 Synthesis and outlook
An interesting result of this study is the different behaviour of the δDw ax as hydrological proxy in the SRZ and in the WRZ. While δDw ax is well-suited as palaeohydrological recorder for terrestrial material sourced in the SRZ, in the WRZ, δDw ax should only be used with care as palaeohydrological recorder. For the WRZ, clearly more research is needed to unravel the factors influencing hydrogen isotope fractionation and δDw ax. Harris et al. (2010) point at a gap between the isotope composition and amount of precipitation in this region, which they attributed to a higher deuterium excess of frontal storm compared to non-frontal storm precipitation.
This suggests that the sparse coverage of climate stations (Cape Town and Johannesburg) used for the interpolated OIPC data set probably does not reflect small spatial-scale changes of δDp. However, the good relationship of OIPC data with interpolated groundwater data in the WRZ may indicate a relatively good representation of δDp. Parallel field studies of collecting precipitation over a certain time period and investigations of δDw ax obtained from plants and soils along different environmental transects (e.g. precipitation amount, altitude, temperature) in the WRZ may help to shed more light onto this issue. Further, the application of a Craig-Gordon leaf water model (Craig and Craig-Gordon, 1965) may be a useful tool to estimate leaf water D-enrichment of certain plant species (e.g. Kahmen et al., 2013a; Berke et al., 2015; Cernusak et al., 2015), its effects on the resulting δDw ax signal and the implications for reconstructing past hydrological changes, especially in the WRZ.
The findings of chapter 5 suggest that changes in the insolation gradient between different latitudes may be important for past environmental changes in the southern African SRZ. The importance of LIG changes on atmospheric circulation systems is raised in climate models (e.g. Davis and Brewer, 2009; Bosmans et al., 2015;
Dallmeyer et al., 2015). However, in palaeoenvironmental reconstruction studies, not only in southern Africa, the process and consequences of changes in the LIG are so far poorly investigated and should receive stronger attention in future palaeoenvironmental reconstruction studies. These long-term changes, however, cannot explain the short-term variations found in the record of this thesis. These short variations may follow from variations of Antarctic sea ice extent or solar activity. High-resolution records from the WRZ covering the whole Holocene could be used to understand the imprints of LIG between high- and mid-latitudes on palaeoenvironmental changes in the WRZ and to unravel the interplay and potential thresholds between forcings dominant in the WRZ and SRZ, respectively.
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