Most common limestones are biogenic. 

Limestone

Dolomite

Caliche

Carbonates come from animals and algae

foraminifera

coccolithophores

molluscs

corals

echinoderms

certain types of algae

very fine-grained limestones

light-colored

Originially laid down as limestone, but due to long periods of exposure to groundwater additional magnesium and sulfur were brought into the beds.

In EXTREMELY evaporitic conditions, dolomite may be able to precipitate directly from seawater.

Subspherical grains of calcium carbonate fored in agitated water conditions.

Associated with shallow, tropical seas. 

Formed when calcium carbonate begins to build up in layers around a nucleus such as a sand grian, or shell fragment.

Frequently have biogenic cores

Currents move the cores back and forth

algae may coat them and help carbonate accumulate

a non-biogenic carbonate formed by the precipitation of calcium carbonate in soils.

NON-CLASTIC!

In arid environments it's caused by water evaportating from the ground bringing carbonates with it.

halite, gypsum and anhydrite

Form from drying water concentrated as salts

May have many compositions

typically formed in terrestrial environments but may also be deposited in marine settings, typically on the shelf.

Defined by clast size and composition

ROUNDING is important

clastic rocks made of grains greater than 2mm in diameter. 

grains: heavily rounded and smooth in conglomerate

Breccia: clasts are angular. 

clastic rocks composed of grains between 2mm and .125mm in diameter

grains: particularly quartz; grains can be seen with the naked eye.

made up of grains between .125mm and .004mm.

grains are commonly made of quartz

small amount between teeth will feel gritty.

clastic mud is formed from clay minerals (similar in structure to tiny mica crystals)

grains are generally smaller than .044mm.

Break along flat planes

will feel smooth against your teeth.

Formed by solution of minerals and precipitation as clay

sediment grains that bounce or jump

as viscosity increases, the size of the particles that can be transported increases.

Water can transport larger particles than air at the same flow velocity.

as speed of flow (and turbulence) increases, the size of particles that can be transported also increases.

As speed (and therefore energy) drops, so does the max particle size in transport.

Dependent on flow velocity, viscosity, fluid depth, and grain size, particles may create ripples, sand waves, dunes, and antidunes.

as fluid velocity increases, so does the scal of the bedform.

relatively small features creaed at relatively low velocities and shallow depths by sand or silt sized particles.

Asymmetrical if formed by unidirectional flow, and symmetrical if formed in oscillating current.

Move with currents and can indicate old current types

broad, low bedforms that range in wavelength from  tens of cm to nearly a 100 m wide.

Straight-crested to highly sinuous in shape.

deposition of suspended sediment; as long as flow is turbulent, smaller particles will remain in suspension, while larger particles fall out of suspension. The resulting sedimentary layer will be graded, with coarser grained material at the bottom that grades into finer and finer particles toward the top. Such deposits occur when muddy water settles.

oblong, raised bulges on the underside of siltstones or sandstones

formed by turbulent, sediment-laden currents scouring a muddy bottom.

only preserved in finer-grained sediments

small impact craters left by raindrops

very common in marine mud; trace fossils created by organisms (often worms) digging through soft sediment.

trace of feeding activity

Skolithos burrow: Vertical burrow type

Diptocraterion Burrow: Dish-shaped infillings in vertical burrows