Geology 1

Front 1

Characteristics of Terrestrial Planets

Back 1

Inner planets, small in size and mass, rocky, solid, dense. Close to the sun. Mostly iron and silicates.

Front 2

Characteristics of Gas Giants

Back 2

Outer planets, huge in size, rings made of dust/debris/ice/rock, very cold and light, made of gas. Thick, deep atmosphere. Mostly hydrogen, helium, NH4, CH4, and ice.

Front 3

Why are the Gas Giants and Terrestrial Planets in their current locations?

Back 3

The planets closer to the sun are hotter and helium and hydrogen are not stable in those conditions (which is what gas giants are made of) and so these gasses burn away in the heat of the sun and leave the solid rocky core (terrestrial planets). The Gas Giants exist far from the sun because that is the only distance away where the gasses remain part of the planet.

Front 4

Layers of the Earth based on chemical composition

Back 4

Crust: silica rich

Oceanic Crust: silica poor--mafic

Mantle: primarily different forms of (FeMg2)SiO4--ultramafic

Core: primarily iron and nickel outer core is liquid

Front 5

Lithosphere

Back 5

crust and upper mantle which is rigid and shatters

Front 6

Asthenosphere

Back 6

Middle above core which flows like plastic

Front 7

Layers of the earth based on how it moves and flows

Back 7

Lithosphere: rigid and shatterable

Asthenosphere: plastic and flows slowly

Mesosphere: rigid

Outer core: liquid

Inner core: rigid

Front 8

Wegener's Continental Drift evidence

Back 8

Continents fit like a puzzle and rock record did not match the current climate--climate belts

Front 9

Pangea

Back 9

One big continent

Front 10

What happens at plate boundaries

Back 10

Plates interact at their boundaries: earthquakes, volcanism, and mountain building

Front 11

How Earth's magnetic field is produced

Back 11

produced by rotation in the spinning flow of the liquid metallic core of iron and nickel creates the magnetic field

Front 12

Paleomagnetism

Back 12

Rocks record the magnetic field when they form in the direction that they form. This changes over time.

Front 13

Sea Floor Spreading

Back 13

Oceanic crust forms along mid ocean ridges and spreads out away from them. This causes the drifting apart of continents

Front 14

Ways two plates can move relative to each other

Back 14

Ddivergent Boundaries: move apart

Convergent Boundaries: move together aka subduction

Transform Boundaries: move sideways, neither created nor destroyed

Front 15

What happens at mid ocean ridges

Back 15

Oceanic plates are created by spreading of the seafloor

Front 16

What happens at a subduction zone

Back 16

Convergent boundaries where one crust goes under another crust causes the crust to be destroyed and melt back into the mantle

Front 17

Atomic Number

Back 17

the number of protons in the nucleus of an atom which determines its chemical properties

Front 18

Molecule

Back 18

A group of atoms bonded together, representing the smallest fundamental unit of a compound that can take part in a chemical reaction

Front 19

Silica formula

Back 19

SiO2

Front 20

Potassium Feldspar

Back 20

KAlSi3O8

Front 21

Pyroxene

Back 21

(Ca,Mg)2Si2O6

Front 22

Olivine

Back 22

(Mg,Fe)2SiO4

Front 23

Calcite (limestone)

Back 23

CaCO3

Front 24

Hematite

Back 24

Fe2O3

Front 25

Pyrite

Back 25

FeS2

Front 26

Gypsum

Back 26

CaSO4 x 2H2O

Front 27

Sodium Chloride

Back 27

NaCl

Front 28

Water

Back 28

H2O

Front 29

Oxygen

Back 29

O2

Front 30

Nitrogen

Back 30

N2

Front 31

Carbon Dioxide

Back 31

CO2

Front 32

Methane

Back 32

CH4

Front 33

Hydrogen Bond

Back 33

intermolecular, weak

Front 34

Covalent bond

Back 34

Intramolecular and the strongest bond

Front 35

Ionic Bond

Back 35

intramolecular; formed when two or more ions of opposite charge attract each other; strong, but most dissolve in water

Front 36

Mineral

Back 36

a naturally occurring, inorganic, solid with a definite chemical composition and an ordered internal structure (crystalline)

Front 37

Characteristics that determine minerals

Back 37

Hardness, luster, color, streak, specific gravity, cleavage

Front 38

Crystals

Back 38

ordered structures and symmetry which is different from a mineral which lacks symmetry

Front 39

Amorphous

Back 39

No symmetry or structure

Front 40

Major categories of minerals

Back 40

Silicates, carbonates, oxides, sulfides, sulfates, halides, hydrates

Front 41

Silicates:

Back 41

tetrahedron structure, commonly joins with other silicate ions (feldspars, quartz)

Front 42

Carbonates:

Back 42

very abundant on Earth's surface, second most important (aragonite)

Front 43

Oxides:

Back 43

oxygen usually ionically bonded to a metal (hematites, magnetite)

Front 44

sulfides:

Back 44

usually bonded to a metal [sulfite ions], important source of ores associated with volcanoes (pyrite)

Front 45

Sulfates:

Back 45

basic unit is the sulfate ion, tetrahedron (anhydrite, barite)

Front 46

Halides:

Back 46

ionic bonded to halogens, salts, toothpaste, lighting, low abundance on earth's surface (salt, fluoride)

Front 47

Major classes of silicate minerals/examples

Back 47

Isolated tetrahedra: zero dimensional (olivine)

sheets: grow out in two dimensions, won't break but peels apart (mica)

chains: grow out in 1 dimension, harder to break but not very durable (pyroxene)

frameworks: 3 dimensional, hardest to break (quartz)

Front 48

Hydrates:

Back 48

contribute to volcano formation, won't combine with oxygen and others (gold, diamond, graphite, sulfur)

Front 49

Difference between minerals and rocks

Back 49

a rock is an aggregate of different minerals and may contain organic remains and mineraloids

Front 50

Info that comes about a mineral's bonds

Back 50

bonds determine physical composition

Front 51

When a mineral crystalizes

Back 51

at equilibrium

Front 52

Metallic Bonds

Back 52

intramolecular bond, when two or more metallic elements share electrons loosely between them, why metals conduct so well

Front 53

Composition of magma

Back 53

Solid: solidified with mineral crystals are carried in the melt

Liquid: the melt itself is composed of mobile ions (mostly Si and O, lesser amounts of Al, Ca, Fe, Mg, Na, K)

Gas: variable amounts of dissolved gas, water vapor, carbon dioxide, and sulfur dioxide

Front 54

What is the difference between magma and lava

Back 54

Lava is magma on the surface

Front 55

Formation of Igneous Rocks

Back 55

they are formed by the removal of energy which is the heat from the magma

Front 56

What can we learn by looking at igneous rocks

Back 56

We can learn where they were formed and the rate of cooling

Front 57

Aphanitic

Back 57

fine grained that the eye cannot see. These cool quickly and form on the surface of the earth--> Extrusive

Front 58

Phanetric

Back 58

Coarse grained which can be seen by the eye. They cool slowly deep in the earth--> Intrusive

Front 59

Porphyritic

Back 59

Both. Fine and coarse grained

Front 60

The color of igneous rock tells us

Back 60

Light colored, higher percentage of silica--> fesic

Dark Colored rocks have low silica but lots of magnesium and iron --> mafic

Front 61

Intrusive Rocks

Back 61

lose heat slowly and grow large crystals. they are formed in the depths of the earth

Front 62

Estrusive Rocks

Back 62

cool at or near the surface but cool too fast to grow crystals

Front 63

Size of crystals in rocks

Back 63

sufficient time, space, and elements

Large crystals form in a tight space with short time and few resources, vice versa

Front 64

Mafic

Back 64

Dark, made of magnesium and iron, hotter

Front 65

Felsic

Back 65

Silica rich, light colored, cooler

Front 66

Bowen's Reaction Series

Back 66

Minerals crystalize in order

Continuous: plagioclase changes from Ca rich to Na rich

Discontinuous: minerals start and stop in an order

olivine

pyroxene

amphibole

mica

muscovite/potassium/feldspar/quartz

Front 67

Temperatures of different magmas

Back 67

felsic (feldspar and silica) 600

intermediate 800

mafic (Mf and Fe rich) 1000

ultramafic 1200

Front 68

What happens to silica content when temperature increases

Back 68

it decreases

Front 69

Rhyolite:

Back 69

fine grained and has a high silica content. formed closer to the surface at 600 degrees

Front 70

Granite:

Back 70

large grained with a high silica content. formed deep in the earth at lowish 600 degree temps

Front 71

Basalt:

Back 71

fine grained with low silica content. formed nearer to the surface at a temperature of around 1000 degrees

Front 72

Gabbro:

Back 72

fine grained with low silica content. formed near the surface at hot temps

Front 73

difference between friction and viscosity

Back 73

friction force of different objects. viscosity is a substance moving over itself

Front 74

Ways viscosity is affected

Back 74

chemical composition: more silica, thicker

temperature: the higher the temp the thinner it is

presence of gasses: more gasses trapped makes for thicker magma

Front 75

Types of volcanoes

Back 75

Shield

Cinder Cones

Strato-Volcanoes

Front 76

Shield Volcanoes

Back 76

largest type, formed by repeated basaltic/mafic flows with little ash, v heavy, low danger

Front 77

Cinder Cones

Back 77

small made of pumice and volcanic glass, dangerous

Front 78

Strato Volcanoes

Back 78

Intermediate size, every typical volcano, silicate rich/felsic/granitic, fueled by subduction zones, most dangerous

Front 79

Pyroclastic flow

Back 79

avalanche of hot glass, pumice, rock, and volcanic glass

Front 80

Lahars

Back 80

ash mixes with rainwater to make concrete like substances that flows down rivers. Causes greatest damage because it happens days later and miles away

Front 81

Mafic/Basaltic Magma

Back 81

less viscous, less silica content, hotter temperature, and gas is able to bubble out. Low explosively and lava flows out little by little as it is able to escape

Front 82

Felsic/Granitic

Back 82

more viscous, higher silica content, lower temperature, thicker and more gasses trapped. High explosively and very danger bc large explosion