**2.2. Continental collision zones**

These strike-slip faults sometimes separate a narrow sliver plate from the remainder of the over-riding forearc plate. Modern examples include the Median Tectonic Line in Japan, the Sumatra Fault in Indonesia, the Denali Fault in Alaska and the Philippine Fault in Philippine (Figure 2). An ancient example can be observed in the Bering Sea [17]. The strike-slip faults in these settings are typically long (hundreds of kilometers) but occasionally segmented [9].

30 Mechanism of Sedimentary Basin Formation - Multidisciplinary Approach on Active Plate Margins

The Median Tectonic Line (MTL) active fault system is the longest and most active arc-parallel, right-lateral strike-slip fault system in Japan [e.g.18, 19]. The MTL extends over a distance of 500 km and accommodates the trench-parallel component of oblique subduction of the

The Great Sumatra Fault is a right-lateral strike-slip fault more than 1900 km in length (Figure 2B). It is related to the northward subduction of the Australian Plate beneath the Sundaland

Strike-slip faulting in Alaska has involved several widely spaced major faults, with an overall seaward migration of activity: the Denali Fault was initiated in the Late Cretaceous or Paleocene and the Fairweather Fault in the Pleistocene (Figure 2C) [23, 24]. These right-lateral strike-slip faults are associated with the Alaskan subduction zone where the Pacific Plate subducts northwestward. Although current strike-slip movement takes place predominantly

The Philippine Fault is a left-lateral strike-slip fault sandwiched between the Manila and Philippine trenches [25–27]. It completely traverses the Philippine archipelago and extends for more than 1000 km (Figure 2D). Several strike-slip basins are developed along releasing bends

**Figure 3.** Indent-linked strike-slip fault systems. (A) North Anatolian Fault (NAF) caused by the collision of the Arabian Plate (AR) with the Eurasian Plate (EU). Abbreviations: EAF, East Anatolian Fault; NEAF, Northeast Anatolian Fault; CF, Chalderan Fault; TF, Tabriz Fault; DSF, Dead Sea Fault; BZFTB, Bitlis–Zagros Fold and Thrust Belt; BS, Black Sea; MTS, Med‐ iterranean Sea; MS, Marmara Sea; AS, Aegean Sea. (B) The Red River Fault (RRF) zone, caused by the collision of the Indi‐ an Plate (IP) with the Eurasian Plate. Abbreviations: SCB, South China Block; SB, Songpan Block; CB, Chuandian Block; ICB, Indochina Block; SF, Sagaing Fault; JF, Jiali Fault; XXF, Xianshuihe–Xiaojiang Fault; LSF, Longmen Shan Fault. Faults and blocks are based on [33]. Plate names: EU, Eurasian; AR, Arabian; NU, Nubia (Africa); AT, Anatolian; SU, Sundaland; BU, Burma; YZ, Yangtze. Maps were drawn using SRTM and GEBCO with plate boundary data [30]. Black, red, and pur‐ ple lines are plate convergent margins, plate-boundary transform faults, and indent-linked strike-slip faults, respective‐ ly. Blue arrows indicate the direction and velocity of plate motion (mm yr-1) relative to the Eurasian Plate based on [31]

on the Fairweather Fault, the Denali Fault also shows some Holocene movement.

Philippine Sea Plate (Figure 2A).

Plate along the Java–Sumatra Trench (Figure 2B) [20–22].

or overstepped faults in this fault zone [28, 29].

Continental collision can cause crustal shortening and thickening by thrusting and escape or by extruding crustal blocks along conjugate strike-slip faults within the plate. These types of collision-related strike-slip faults between continental blocks are classified as indent-linked strike-slip faults (Figure 1) [9].

Modern examples include several strike-slip faults in Turkey where the Arabian Plate is converging with the Eurasian Plate, and in southern China where the Indian Plate is colliding with the Eurasian Plate (Figure 3). In the latter example, the collision originally formed the left-lateral Red River Fault associated with the southeastward extrusion of the Indochina Block [32]. After the propagation of the indent, the South China Block was extruded along the preexisting Red River Fault as a block boundary with right-lateral movement.

**Figure 4.** Plate-boundary transform fault systems. (A) Alpine Fault (AF) in New Zealand. Abbreviations: HF, Hope Fault; WF, Wairau Fault; NIDFB, North Island Dextral Fault Belt; HT, Hikurangi Trough; PT, Puysegur Trench. Faults are from [34] and [35]. (B) San Andreas Fault systems (SAF) in North America. Abbreviations: DV, Death Valley; RB, Ridge Basin; ST, Salton Trough; GC, Gulf of California; BC, Baja California Peninsula. (C) Dead Sea Fault systems. Abbreviations: DS, Dead Sea; GA, Gulf of Aqaba; LR, Lebanon Range; ALR, Anti-Lebanon Range. Plate names: PA, Pacific; AU, Australian; NA, North American; JF, Juan de Fuca; AR, Arabian; NU, Nubian (African). All maps were drawn by using SRTM and GEBCO with plate boundary data [30]. Black, red, and purple lines are subduction zones, oceanic spreading ridges, and plate-boundary transform faults, respectively. Blue arrows indicate the direction and velocity of relative plate mo‐ tion (mm yr-1) based on [31]

#### **2.3. Plate-boundary transform zones**

Plate-boundary transform faults develop between two plates rotating around the poles that define the relative motion between them [9]. The San Andreas Fault, Dead Sea Fault, Alpine Fault (New Zealand), and the northern and southern margins of the Caribbean Plate are modern examples of this type (Figure 4).
