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These terms refer to the crystalline structure of the minerals that are present in a body of rock. Rocks with an interlocking mineral structure have formed from melt or from recrystallization and therefore are igneous or metamorphic. Their crystals have formed in a set order of crystallization, filling the spaces fully between them. Examples are granite, basalt, schist, and phyllite.

Non-interlocking rock structures are usually clastic sedimentary rocks, which are formed from the compaction and cementation of rock particles of various types. Compaction and cementation will leave air and fluid spaces between rock particles which, although cemented together, are not interlocking. Examples are sandstone, limestone, and shale.

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What does non interlocking mean?

Non-interlocking rock texture is a characteristic of clastic sedimentary rock, where particles of sediments have been cemented together by precipitated minerals. The particles may be loosely cemented, with spaces between particles. Rocks of this type tend to be 'soft' in that they are broken easily. An interlocking crystalline rock structure is formed by the progression of crystallization temperatures of various minerals as they form from solidifying magma. The solidification temperatures of the mineral constituents vary, and the last to crystallize is usually quartz, which infills any voids that remain. The resultant mineral structure is compact, hard, and resistant to weathering.


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