“…Modeling 230 Th in the ocean began with 1-D analytical models (Bacon & Anderson, 1982;Clegg et al, 1991;Nozaki et al, 1981;Nozaki & Horibe, 1983;Roy-Barman et al, 1996), which demonstrated that only reversible scavenging was able to reproduce the observations of both the dissolved and particulate vertical profiles. To explain complex (nonlinear) 230 Th profiles, more elaborate box models were developed that could account for different transport conditions and particle regimes under different ocean conditions, such as upwelling of deep water masses in the Southern Ocean (Chase et al, 2003;Roy-Barman et al, 2019;Rutgers van der Loeff et al, 2016;Rutgers van der Loeff & Berger, 1993;Venchiarutti et al, 2011), convection of deep water masses in the North Atlantic (Moran et al, 1995(Moran et al, , 1997Vogler et al, 1998), and lateral exchange between open ocean and ocean margin regimes (Anderson et al, 1983;Roy-Barman et al, 2009). More recently, 230 Th has also been integrated into complex geographic schemes in 2-D models (Luo et al, 2010;Marchal et al, 2000), in 3-D models of intermediate complexity (Henderson et al, 1999;Missiaen et al, 2019;Rempfer et al, 2017;Siddall et al, 2007Siddall et al, , 2005, and in global climate models (GCMs) (Dutay et al, 2009;Gu & Liu, 2017;Rogan et al, 2016;Van Hulten et al, 2018).…”