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Fold a ymmetry, isoclinal and recum bent fo ld s, and low-angle reverse faults are un  mistakabl e indicators of geologic lran port directio n. Some of the tr<msport took place by gravity sliding when th e sediments were still uncon o lidated, but the majority was caused by tectoni c processes. Five o f th e s ix major geologic settings may account for the transport directions determined in metasediment s of various age groups of Pen insular Ma lays ia. Convergent transport occurs on li mbs of anti clinori a. Di vergent tran sport directions occur on limbs of warps deve loped by ve rti cal uplift and in sediments th at have been pressed out from s ires between colljdin g contin ental pl ates. Three cases ofunidiJ·ect ional tran sport are possibl e and consi t of overthrust and thrusts, subducti on, and obduction. There is no indication that obduction ever to ok pl ace in the penin sul a. Cross-cutting structures. different fold sizes, and re fold ed fold s are th e main crit eria for dererminjng the re lative ages of transport direction s. From older to younger transport d irections th e movement was eastward , followed by movement towards south, then in a general westward ilirection (whi ch is present in all geologic domai ns) , succeeded by one towards east, and concluded by transport in soULh to south east direction . The general westward transport probably took place during th e Late Triassic-Early Jurassic deformation period and is interpreted as a consequence of eastward subducti on of th e Indi an Ocean plate beneath the Euras ian plate in the vicinity of th e peninsula. The ca use of southward transport that probably occurred in two different deformation phases is an e n.i gma.

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