Physical weathering, also called mechanical weathering or disaggregation, is the class of processes that causes the disintegration of rocks without chemical change. The primary process in physical weathering is
abrasion (the process by which
clasts and other particles are reduced in size). However, chemical and physical weathering often go hand in hand. Physical weathering can occur due to temperature, pressure, frost etc. For example, cracks exploited by physical weathering will increase the surface area exposed to chemical action, thus amplifying the rate of disintegration.
Abrasion by water, ice, and wind processes loaded with sediment can have tremendous cutting power, as is amply demonstrated by the gorges, ravines, and valleys around the world. In glacial areas, huge moving ice masses embedded with soil and rock fragments grind down rocks in their path and carry away large volumes of material. Plant roots sometimes enter cracks in rocks and pry them apart, resulting in some disintegration; the burrowing of animals may help disintegrate rock However, such biotic influences are usually of little importance in producing parent material when compared to the drastic physical effects of water, ice, wind, and temperature change.
Thermal stress weathering (sometimes called insolation weathering)
 results from the expansion and contraction of rock, caused by temperature changes. For example, heating of rocks by sunlight or fires can cause expansion of their constituent minerals. As some minerals expand more than others, temperature changes set up differential stresses that eventually cause the rock to crack apart. Because the outer surface of a rock is often warmer or colder than the more protected inner portions, some rocks may weather by
exfoliation – the peeling away of outer layers. This process may be sharply accelerated if ice forms in the surface cracks. When water freezes, it expands with a force of about 1465 Mg/m^2, disintegrating huge rock masses and dislodging mineral grains from smaller fragments.
Thermal stress weathering comprises two main types,
thermal shock and
thermal fatigue. Thermal stress weathering is an important mechanism in
deserts, where there is a large
diurnal temperature range, hot in the day and cold at night.
 The repeated heating and cooling exerts
stress on the outer layers of rocks, which can cause their outer layers to peel off in thin sheets. The process of peeling off is also called exfoliation. Although temperature changes are the principal driver, moisture can enhance
thermal expansion in rock.
Forest fires and range fires are also known to cause significant weathering of
rocks and boulders exposed along the ground surface. Intense localized heat can rapidly expand a boulder.
The thermal heat from wildfire can cause significant weathering of rocks and boulders, heat can rapidly expand a boulder and thermal shock can occur. The differential expansion of a
thermal gradient can be understood in terms of stress or of strain, equivalently. At some point, this stress can exceed the strength of the material, causing a crack to form. If nothing stops this crack from propagating through the material, it will result in the object's structure to fail.
A rock in
, Sweden fractured along existing
possibly by frost weathering or thermal stress
Parts of this article (those related to conflating frost weathering and frost wedging and also not incorporating hydrofracturing which makes the science here seem wrong See paper = Matsuoka, N.; Murton, J. 2008. "Frost weathering: recent advances and future directions". Permafrost Periglac. Process. 19: 195–210. doi:10.1002/ppp.620 referenced on Frost weathering page) need to be updated. (January 2018)
Frost weathering, frost wedging, ice wedging or cryofracturing is the collective name for several processes where ice is present. These processes include frost shattering, frost-wedging and freeze–thaw weathering. Severe frost shattering produces huge piles of rock fragments called
scree which may be located at the foot of mountain areas or along slopes. Frost weathering is common in mountain areas where the temperature is around the freezing point of water. Certain frost-susceptible soils expand or
heave upon freezing as a result of water migrating via
capillary action to grow
ice lenses near the freezing front.
 This same phenomenon occurs within pore spaces of rocks. The ice accumulations grow larger as they attract liquid water from the surrounding pores. The ice crystal growth weakens the rocks which, in time, break up.
 It is caused by the approximately 10% (9.87) expansion of
water freezes, which can place considerable stress on anything containing the water as it freezes.
Freeze induced weathering action occurs mainly in environments where there is a lot of moisture, and temperatures frequently fluctuate above and below freezing point, especially in
periglacial areas. An example of rocks susceptible to frost action is
chalk, which has many pore spaces for the growth of ice crystals. This process can be seen in
Dartmoor where it results in the formation of
tors. When water that has entered the joints freezes, the ice formed strains the walls of the joints and causes the joints to deepen and widen. When the ice thaws, water can flow further into the rock. Repeated freeze–thaw cycles weaken the rocks which, over time, break up along the joints into angular pieces. The angular rock fragments gather at the foot of the slope to form a
talus slope (or scree slope). The splitting of rocks along the joints into blocks is called block disintegration. The blocks of rocks that are detached are of various shapes depending on rock structure.
Wave action and water chemistry lead to structural failure in exposed rocks
Coastal geography is formed by the weathering of wave actions over geological times or can happen more abruptly through the process of salt weathering.
Pressure release could have caused the exfoliated granite sheets shown in the picture.
In pressure release, also known as unloading, overlying materials (not necessarily rocks) are removed (by erosion, or other processes), which causes underlying rocks to expand and fracture parallel to the surface.
Intrusive igneous rocks (e.g.
granite) are formed deep beneath the Earth's surface. They are under tremendous pressure because of the overlying rock material. When erosion removes the overlying rock material, these intrusive rocks are exposed and the pressure on them is released. The outer parts of the rocks then tend to expand. The expansion sets up stresses which cause fractures parallel to the rock surface to form. Over time, sheets of rock break away from the exposed rocks along the fractures, a process known as
exfoliation. Exfoliation due to pressure release is also known as "sheeting".
Retreat of an overlying glacier can also lead to exfoliation due to pressure release.
Salt crystallization, otherwise known as
haloclasty, causes disintegration of rocks when
saline solutions seep into cracks and joints in the rocks and evaporate, leaving salt
crystals behind. These salt crystals expand as they are heated up, exerting pressure on the confining rock.
Salt crystallization may also take place when solutions
decompose rocks (for example,
chalk) to form salt solutions of sodium
sodium carbonate, of which the moisture evaporates to form their respective salt crystals.
The salts which have proved most effective in disintegrating rocks are
magnesium sulfate, and
calcium chloride. Some of these salts can expand up to three times or even more.
It is normally associated with
arid climates where strong heating causes strong evaporation and therefore salt crystallization. It is also common along coasts. An example of salt weathering can be seen in the
honeycombed stones in
sea wall. Honeycomb is a type of
tafoni, a class of cavernous rock weathering structures, which likely develop in large part by chemical and physical salt weathering processes.
Biological effects on mechanical weathering
Living organisms may contribute to mechanical weathering (as well as chemical weathering, see 'biological' weathering below).
mosses grow on essentially bare rock surfaces and create a more humid chemical microenvironment. The attachment of these organisms to the rock surface enhances physical as well as chemical breakdown of the surface microlayer of the rock. On a larger scale, seedlings sprouting in a crevice and plant roots exert physical pressure as well as providing a pathway for water and chemical infiltration.