Abstract: The Eyre Peninsula, South Australia, makes up the southern part of the Gawler Craton. It contains a major portion of Archean to mid-Proterozoic crystalline basement province of the Gawler Craton. It is a region which, except minor, localized movements, has been a reasonably stable platformal area since it was stabilized before 1423 Ma. The north-eastern parts of the craton are unconformably overlain by Late proterozoic and Cambrian platform sediments deposited on the Suart Shelf. The Adelaide Geosyncline, which now forms the Delamarian Fold Belt, provides the north-eastern boundary for the Gawler Craton and the Suart shelf. The eastern boundary developed between 800-490 Ma and is actually delineated by the Torrens Hinge Zone. The Gawler Craton has been subjected to substantial extension 2000 Ma. This formed a sedimentary basin into which to Hutchison Group was deposited. The Kimban Orogeny (1840- 1550 Ma) was associated with intrusive magmatism and deformed the new intrusives, the Hutchison Group and the underlying basement. The Paleoproterozoic Kimban mobile belt was exposed in the study area and divides the area into two contrasting crustal terrains juxtaposed by the Kalinjala Shear Zone. The western terrain consists of the Hutchison Group meta-sediments (1964- 1845Ma), meta-basics and mete-volcanics, and the Moody Granitoid Suite (1740- 1700Ma). The Hutchison Group unconformably over1ies the older Sleaford Complex which was affected by the Sleafordian Orogeny (2600- 2400Ma) as well as the Kimban Orogeny. The eastern terrain essentially consists of a batholith, here referred to as the Lincoln Batholith, composed of the Donington Granitoid Suite (185O-1843 Ma), mafic dykes that syn-plutonic with the Donington Granitoid Suite, and the Colbret Granitoid Suite. The Lincoln Batholith is intruded by the Tournefort mafic dyke suite. The mafic dykes and the mylonite in Jussieu Peninsula are mainly exposed along the coastal section. Although they are deformed, boudinaged and recrystallized, their development in an environment of transtensional and transpressional tectonic settings can still be recognized. By using transfer geometry, we can explain the propagation and intrusion of the mafic dykes, the deformation along the mafic dyke boundaries, and localization of deformation that formed the ductile mylonite zone.