Most recently studies have started to show agriculturally related alluviation in sub-Saharan Africa particularly Mali ( Lespez et al., 2011 and Lespez et al., 2013) but these studies are in their infancy and complicated by the ubiquity of herding as an agricultural system. Similarly

Baf-A1 mouse very few studies have investigated Holocene alluvial chronologies in SE Asia and also pre-European Americas. However, many studies have shown that the expansion of clearance and arable farming in both Australia and North America is associated with an unambiguous stratigraphic marker of a Holocene alluvial soil covered by rapid overbank sedimentation ( Fanning, 1994, Rustomji and Pietsch, 2007 and Walter and Merritts, 2008). This change in the driving factors of sediment transport has practical implications through rates of reservoir sedimentation which have now decreased sediment output to the BMS-387032 nmr oceans (Sylvitski et al., 2005) and sediment management issues. Humans now are both the dominant geomorphological force on the Earth and by default are therefore managing the Earth

surface sediment system (Hooke, 1994, Wilkinson, 2005 and Haff, 2010). The implications go as far as legislation such as the Water Framework Directive in Europe (Lespez et al., 2011). Indeed awareness of human as geomorphic agents goes back a long way. In the 16th century Elizabeth I of England passed an act seeking to control mining activities on Dartmoor in order to prevent her harbour at Plymouth from being silted up. Our role was more formally recognised by G P Marsh, one of the first geomorphologists to realise the potential of human activities in Gilbert’s (1877) classic study

of mining in the Henry Mountains, USA. If we accept that there is a mid or late Holocene hiatus in the geological record within fluvial systems that is near-global and associated with human activity, principally agricultural intensification, then this would be a prima-facie case for the identification of a geological boundary with an exemplary site being used as a Global Stratigraphic Section Ureohydrolase and Point (GSSP). The problem is that this boundary of whatever assigned rank would be diachronous by up to approximately 4000 years spanning from the mid to late Holocene. In geological terms this is not a problem in that as defined on a combination of litho, bio and chronostratigraphic criteria the finest temporal resolution of any pre-Pleistocene boundaries is approximately 5000 years. However, the Pleistocene-Holocene boundary has a far higher precision either defined conventionally, or as it is now from the NGRIP δ18O record (Walker et al., 2009). It would also be difficult to define it with less precision than stage boundaries within the Holocene sensu Walker et al. (2012) and Brown et al. (2013). This leaves two principal alternatives.