2.1: Weathering

Physical Weathering

Physical weathering occurs when existing rocks are mechanically broken into smaller pieces with little or no chemical change. The most important types of physical weathering include freeze-thaw (expansion of cracks via freezing of water), biological activity, changes in volume via wetting and drying (especially important with mudrocks), and stress relief weathering. Locally, physical weathering via thermal expansion and contraction and the growth of salt crystals may be important in deserts and coastal areas, respectively.

Figure \(\PageIndex{1}\): Examples of physical weathering. A) Boulder split by frost wedging (Dominicus Johannes Bergsma via Wikimedia Commons; CC BY-SA 4.0), B) Tree roots can enhance existing fractures (Don Graham via Wikimedia Commons; CC BY-SA 2.0), C) Half Dome in Yosemite National Park is an exfoliation dome caused by stress relief weathering (HylgeriaK via Wikimedia Commons; CC BY-SA 3.0), D) Salt weathering happens when salt water spray blows on to porous rocks. When the water evaporates, salt crystals grow and break apart connections between grains (Bagamatuta via Wikimedia Commons; public domain).

 

Chemical Weathering

Chemical weathering is the chemical and/or mineralogical alteration of a rock; it can take place via in situ alteration of minerals or by the removal/relocation of dissolved substances.

Solution (aka dissolution) is a type of chemical weathering that takes place when material is dissolved in water, a processes that is commonly assisted if the water is slightly acidic. Common examples of dissolution include halite in water and the dissolution of marble by acid rain.

Hydrolysis is a type of chemical weathering that takes place when acid and water react with a mineral to form clay minerals, silica, and to release ions into solution (commonly K, Na, and Ca). The most common example is the weathering of feldspar to form clay, a process that results in large amount of fine-grained particles and dissolved material.

Oxidation occurs when compounds lose or share electrons with oxygen, the transformation from pyrite to hematite is a common and important example.

Figure \(\PageIndex{2}\): Types of chemical weathering. A) 800 years of solution weathering have made this marble tombstone almost illegible (Palauenc05 via Wikimedia Commons; CC BY-SA 4.0), B) The light colored layers within this bed of coal are bentonites, which from when feldspar-rich volcanic ash undergoes hydrolysis and transforms into clay (Michael C. Rygel via Wikimedia Commons; CC BY-SA 3.0), C) Acid mine drainage discharging from an exposed shaft in an abandoned coal mine. Oxidation of pyrite (FeS₂) causes the precipitation of orange ferric hydroxide (FeOH₃) seen in the foreground (Michael C. Rygel via Wikimedia Commons; CC BY-SA 3.0)

The processes of physical and chemical weathering commonly act together to speed the breakdown of rocks and minerals. Fractures formed by physical weathering can dramatically increase the surface area of a rock. The increase in surface area makes more of the rock available for chemical weathering to act on, which may result in further physical destruction of the rock. This interrelationship of physical and weathering can be seen in when fractured blocks develop rounded corners (spheroidal weathering); the increased surface area to volume ratio near the corners results in preferential weathering. Deeply weathered rocks commonly develop a rounded shape because a sphere has the lowest surface area to volume ratio of any shape.

Figure \(\PageIndex{3}\): Notable patterns and processes caused by weathering. A) Spheroidal weathering happens as weathering preferentially acts on the corners and edges of rocks. The longer these fractured rocks are exposed the more round they become (Joachim Himmeröder via Wikimedia Commons; CC BY-SA 2.0 DE), B) Physical and chemical weathering are acting together to degrade this once details sandstone sculpture (Slick via Wikimedia Commons; CC0 1.0)

Some Generalizations

CLimate, Organisms, Relief, Parent material, and Time are the variables that influence the weathering of rock and the creation of the resulting soils; the acronym CLORPT is commonly used to remember these processes (Jenny, 1941, Factors of Soil Formation). Climate, particularly temperature and precipitation, probably exerts the most profound influence by controlling the type, speed, and nature of chemical weathering. Despite the complexities inherent in the system, generalizations can be made:

• Because rocks and minerals are most stable under conditions closest to those under which they formed, Bowen’s Reaction Series provides a general framework for predicting igneous rocks' resistance to chemical weathering. Iron-rich ultramafic rocks formed at high temperatures are particularly prone to chemical weathering; silica-rich felsic rocks and minerals formed at relatively low temperatures tend to be the most resistant.
• Quartz, rutile, anatase, magnetite, and zircon are some of the most common stable minerals formed from melts.
• With the notable exception of chert, minerals formed by precipitation (halite, gypsum, etc.) tend to be easily dissolved and prone to weathering.
• Feldspars are prone to hydrolysis and are rapidly destroyed in humid climates.
• Sandstones are common ridge-formers in humid climates; Carbonates are common ridge-formers in arid and semi-arid climates but are valley-formers in humid climates
• Generally speaking, increasing the temperature and the amount of liquid water tends to increase chemical weathering rates.