<p>It is now well-established that the Earth&#8217;s mantle and lithosphere form an integrated, dynamically self-regulating system. Numerical convection models that self-consistently generate plate-like behavior are a powerful tool to investigate this system, but have only recently reached a level at which they can be linked to the geodynamics of the Earth. Strongly temperature-dependent and viscoplastic rheology is known to be a key ingredient for these models to be successful. Such rheologies, however, are typically time-independent and lack a memory on the previous history of deformation. Yet, it is known that the Earth&#8217;s geodynamic evolution is somewhat guided by structures of pre-existing weakness, which was initiated a potentially long time before.</p><p>As a step forward we implement a simple form of rheological memory in the mantle convection code <em>StagYY</em>: strain weakening [<em>Fuchs & Becker, 2019,</em> <em>Role of strain-dependent weakening memory on the style of mantle convection and plate boundary stability</em>, <em>Geophys. J. Int., 218, 601-618</em>]. We present calculations in 2D cases with and without continents, and also selected 3D cases. By varying the governing parameters for plate-like behavior as well as the rates of rheological damage and healing, we examine how strain weakening modifies the generation of plate-like behavior and its time dependence as well as the drift of continents.</p><p>First results indicate the importance of the balance of weakening (via the critical strain) and thermal healing. The averaged cumulative strain (effectively the degree of lithospheric weakening) is lower when healing is more effective, so that plastic failure of the lithospheric and the formation of new plate boundaries is complicated, as expected. In initial models with strong, long-living continents, accumulated strain is very small within the continents and seems insufficient to induce substantial weakening, even if the memory on previous deformation is infinite (i.e. no healing with continents). Further models with weaker continents and different rheological parameters will be presented.</p>
Feedbacks between a non-Newtonian upper mantle, mantle viscosity structure and mantle dynamics
