## 5 Discussion  
### Depositional Setting  
The study area consists of a deep-water fan system starting from the area of the channels, levees, lobes, and basin plains. All facies associations collect to form a depositional environment based on zones 1, 2, 3, and 4 of the deep-water depositional environment (Figure 8). Zone 1 is the inner fan, consisting of the channel-levees complexes (Figure 8). This proximal area receives its sediments from the canyon and experiences high-density turbidite currents that can transport and deposit sediments ranging in size from coarse sand to medium sand, forming a fining-upward sequence pattern (Figure 8). The proximal area faces a hypoconcentrated density flow where the flow is associated with the matrix strength and grain friction [15]. The density of the flow causes the presence of erosion and records the sharpness and eroded bed (Figure 9). This zone can be a good hydrocarbon accumulation area because it has a high sand content, thick sediment thickness, and good sorting properties with a wider diameter distribution [52]. Figure 8: The depositional setting for each component of the facies association interpreted in the study area. Channel shows a fine-upward sequence located in the inner fan (zone 1) part; the levee shows a fine-upward sequence located in the outer channel in the inner and mid fan (zone 1 and zone 2); the channelized lobe shows a coarsening-upward sequence located in the proximal lobe with the presence of a distributary channel, which can be found in the mid fan (zone 2); the distal lobe/non-channelized lobe shows the coarsening-upward sequence located in the distal lobe and no distributary channel are present, which can be found in the outer fan (zone 3); the basin plain is located in the outer of the turbidite fan system. Zone 2 is the middle fan section consisting of lobes (Figure 8). The lobes in zone 2 consist of channelized lobes and non-channelized lobes. Channelized lobes are distinguished by the presence of channels/distributancy channels in the vertical sequence upward of the sedimentary log, as shown in L4 (Figure 7), whereas non-channelized lobes are perceived by the absence of channel sequences in the interpreted vertical sequence. These channelized lobes have a sandstone lithology (f1 and f2) with a medium to thin thickness and a fining-upward sequence pattern and are usually located in the upper lobe (lobe axis) (Figure 8). However, non-channelized lobes are usually located around the proximal lobe to the end lobe, as shown in L1 (Figure 6). These lobes do not show any combination of fining-upward sequence patterns in the entire vertical sequence. This pattern is usually formed by the spreading of the tips of the distributary channels in the upper part of the lobe. However, if there are any edges or slopes in that area, zone 2 is reachable by the tips of distributary channels. Zone 2 is located in front of zone 1, and their sediment transportation depends on medium to high-density turbidity currents, as well as debris currents (Figure 9). The basis of their sediments support mechanism is equivalent to the concentrated density flows which possess both hypoconcentrated and turbidity current characteristics [15; 53]. The medium to high-density turbidite currents was proficient in depositing medium-sized sand sediments with a medium thickness (thickness less than zone 1), good to moderate sorting, and low-matrix content (Figure 10). The transportation of this medium-density turbidity current results in sediment characteristics that have a low-matrix content, high authigenic content, high porosity, and permeability [54]. The entire zone exhibits coarsening-upward sequence characteristics, whereas the presence of distributary channels in the lobes indicates a fine-upward sequence pattern within a vertical coarsening-upward sequence. Figure 9: Summary of a depositional model for the northern part of the Crocker Formation.