Buton Island is part of the microcontinent that is part of the North Australian Continent. This causes the island's stratigraphy to have similarities with the islands in East Sulawesi (Banggai Sula) and the Banda Arc (Seram Island, Kai, Tanimbar, Timor).

Stratigraphy is divided into four tectonic or sedimentological events, Pre-Rift sedimentation, Rift-Drift sedimentation, syn and post orogenic sedimentation, and recent orogenic sedimentation. Hamilton (1979) stated in Davidson (1991) that the Muna-Buton area is composed of two different micro-continent fragments, namely the eastern part of Buton Island and Tukang Besi in the east and the western part of Buton and Muna Island in the west. This seems to be proven by the results of the interpretation of the regional anomaly of gravity map, even though the scope of this research area does not extend to Tukang Besi. The western part is strongly influenced by continental crust (granitic) while the eastern part is strongly affected by the composition of the banda sea crust (basaltic). In relation to the pattern of the existence of sedimentary basins, based on this study it is shown that there are several interesting depocenters (sub-basins) and elevations. The distribution of the sedimentary sub-basins and elevations is somewhat different from that stated by Davidson (1991).

Based on the three exploration wells, namely Sampolaka-1S, Bulu-1S and Bale-1S, all three were discovered empty or dry even though there were indications of hydrocarbons. Based on the regional gravity anomaly map, the positions of the Sampolaka-1S and Bulu-1S wells are in a strong suture zone so that the hydrocarbons are not trapped. While the Bale-1S well is on the edge of the depocenter. Based on the interpretation of the gravity anomaly map, the remaining possible traps/structures that are more interesting are in the southern part of Muna Island and southwest of Buton, the east-central coast of Muna Island to the north and west of Ereke, which used to be called the Lambele Sub-basin. Oil seeps, gas seeps and asphalt are very abundant on Buton Island. Asphalt is widespread in North Buton and South Buton. Gas seeps are located on Wawoni Island, North Buton and Central Buton. The gas is biogenic. Oil seeps were found in Nunu Village (Central Buton) and South Buton. On Muna and Wawoni Islands, there were no indications of hydrocarbons. The results of the GC analysis of the Nunu oil seep showed that the chromatogram had undergone biodegradation. All the alkanes and their isoprenoids have been lost for consumption by aerobic bacteria. It is estimated that the Nunu oilseepage sample has undergone biodegradation with a level of 4-5 (moderate). Gas seepage is very common in North Buton. Its characteristics are associated with hot springs adjacent to shear faults. Asphalt in Buton is controlled by structures and is located near or on reactivated Miocene faults or Pliocene-Pleistocene faults, especially in the South Buton area. Based on geochemical analysis, the types of oil in Buton are divided into two that are Mesozoic and Cenozoic oils. In the research area, at the North Buton region, the source rock is carbonate marine shale of the Late Triassic Winto Formation, which has been shown to correlate with several hydrocarbon seeps that appeared on Buton Island. In addition, the Miocene Shale of the Tondo Formation has the potential to become host rock in this area, which is proven to correlate with Nunu oil seeps that are present in the Buton fault line. Reservoir potential in this area comes from limestone of the Tobelo Formation of Cretaceous – Paleogene age, sandstones and limestones of the Tondo Formation of Miocene age, and sandstones of the Trias – Jurassic age of the Meluhu Formation. In addition, there is potential for the Kapantoreh fractured ophiolite, which can be found close to the west along the Buton fault. Structural traps are generally in the form of 3-way dip and 4-way dip associated with up faults and folds. Structural traps were generally formed in the Late Miocene. In North Buton, structural traps are associated with the fold-thrust belt. Stratigraphic traps can be found in the Tondo Formation (Miocene), in the form of changes in limestone facies with claystone.