plains of Guinevere is a deformation zone that is made up of discontinuous segments of lineament belts and ovoids that are referred to as the Beta-Eistla deformation zone. Other structural features are observed in coronae and coronae-like features as well as tesserae and other highly tectonized units. Within this region, structures exhibit a diversity of orientations and occur in sets of features with similar trends. Prominent East-West and Southeast-Northwest trends are locally observed in the regional plains. The figure to the left, beginning with A, shows a backscatter image of the northeastern region of Guinevere Planitia. Depicted in figure B, in the shaded regions are outcrops of tesserae which are concentrated on the eastern side of Beta Regio. Wrinkle ridges can be viewed as the purple fill in figure C. These outcrops dominate the low-lying region and are marked with yellow lines that represent major trends. Figure D shows the distribution of fracture belts and their trends in black. The likely cause of these trends is due to mantel upwelling at Beta Regio to the west. The trend of these figures can be directly related to radiating fractures and grabens, interpreted as underlying dyke swarms. The remainder of the systems are interpreted to be caused by tectonic stresses related to uplift or a combination of dyke and uplift mechanisms. Volcanology Volcanism is one of the fundamental processes of heat transfer from planetary interiors. By assessing the location of volcanic deposits and edifices, their volumes, and their sequences provide evidence for quantitative assessment of heat transfer in space and time. The region contains three major volcanoes which have smaller volcanic constructs built upon their flanks and summit regions: Atanua, Rhpisunt, Tuli, and Var Mons, and three coronae: Hulda, Madderakka, and Pölöznitsa. Due to the amount of flows from these major eruptive centers, there is much obscurities among the deposits. Relative age relationships both within and between the major eruptive centers are difficult to determine due to the complex nature in which these flows coalesce and inter-finger. Each volcano appears to have had an extensive period of eruptive activity with several major phases creating large flow fields and more localized activity occurring both at vents on the flanks of the volcanoes and at their summits. Geologic mapping shows a general progression from upland terrain to volcanic plains and then to shield volcanoes and flow fields but also reveals a complex interplay between