DAY 2 Mineralogy Flashcards

1
Q

when did the mohs scale established

A

1824

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2
Q

when was mohs hard scale invented?

A

1894

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3
Q

who invented the mohs scale?

A

frederic m

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4
Q

who invented the mohs scale?

A

frederic mohs

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5
Q

who invented mohs scale

A

frederic mohs

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6
Q

how man

A
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7
Q

transition elements within crystal lattices that can change the color of a mineral

A

chromophores

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8
Q

transition elements within crystal lattices that can change the color of a mineral

A

chromophores

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9
Q

how many silicates in mohs scale

A

4 talc orthoclase feldspar quartz topaz

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10
Q

how many hydrous in mohs scale

A

4 talc gypsum apatite topaz

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11
Q

how many hexagonal in mohs scale

A

calcite apatite quartz corundum

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12
Q

how many isometric in mohs scale

A

2 fluorite and diamond

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13
Q

how many isometric in mohs scale

A

2 fluorite and diamond

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14
Q

how many orthorhombic in mohs scale

A

1 topaz

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15
Q

how many monoclinic in mohs scale

A

3 talc gypsum orthoclase feldspar

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15
Q

how many orthorhombic in mohs scale

A

1 topaz

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15
Q

how many isometric in mohs scale

A

2 fluorite and diamond

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15
Q

ratio of velocity of light in air and the velocity of light in a medium

A

refractive index

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15
Q

this has a single refractive index

A

isotropic minerals

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15
Q

more than one refractive index

A

anisotropic minerals

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15
Q

property of a mineral that can produce a “double image” of an object behind the mineral due to light passing through the mineral having two polarized rays vibrating at right angles from each angle

A

double refraction

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16
Q

minerals that are deformed through compressive stress

A

malleable

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17
Q

also called hypdiomorphic hypautomorphic sub idioblastic

A

suhedral

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18
Q

also called allotriomorphix xenomorphic xenoblastic

A

anhedral

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19
smallest unit of pattern that when repeated by a set of symmetry operations will generate the long range pattern characteristics of crystal
motif
20
point used to represent any motif
node
21
set of rules that govern the repetition of motifs which can produce two or three dimensional patterns with long range order
symmetry operations
22
specific length and direction of systematic displacement by which the pattern is repeated
unit translation vector
23
smallest units of meshes which contains at least one node and the unit translation vectors
unit meshes
24
groups denoted by their rotational and reflection symmetry
plane point groups
25
combines translation parallel to an axis with rotation about the axis
screw rotation
26
how many plane lattice groups
17
27
recognized groups that are based on the total symmetry of their plane lattices
plane lattice groups
28
3d equivalents of the 2d plane point groups
space point groups
29
3d patterns of points produced from the translation of nodes of space point groups
space lattices
30
defined on the basis of the external symmetry of mineral crystals and belong to six crystal systems with its own characteristic symmetry
crystal classes
31
parallelipiped whose edge lengths and volume are defined by the 3 unit translation vectors
unit cell
32
orientation of the unit cell edge
crystallographic axes
33
consists of a 3d set of one or more crystal faces that possess similar relationship to the crystallographic axes
crystal forms
34
encloses a mineral specimen and exist alone in perfectly formed euhedral crystals and also include all forms in the isometric system and many forms in the tetragonal hexagonal trigonal and orthorhombic systems
closed crystal form
35
what are the crystal class of isometric?
hexoctahedral hextetrahedral gyroidal dipyroidal tetraoidal
36
what are the crystal class of tetragonal?
ditetragonal-dipyramidal ditetragonal-pyramidal tetragonal scalenohedral tetragonal trapezohedral tetragonal dipyramidal tetragonal disphenoidal tetragonal pyramidal
37
what are the crystal class of hexagonal?
dihexagonal dipyramidal dihexaginal pyramidal ditrigonal dipyramidal hexagonal trapezohedral hexagonal dipyramidal hexagonal pyramidal trigonal dipyramidal
38
crystal class of rhombohedral/trigonal
hexagonal scalenohedral ditrigonal pyramidal trigonal trapezohedral trigonal pyramidal rhombohedral
39
crystal class of orthorhombic?
rhombic ipyramidal rhombic pyramidal rhombic disphenoidal
40
crystal class of monoclinic?
prismatic sphenoidal domatic
41
crystal class of triclinic?
pinacoidal pedial
42
consists of a single face
pedion
43
a pair of parallel faces
pinacoid
44
has 3 parallel to an axis
prism
45
has 3 or more faces that intersect at an axis
pyramid
46
a pair of faces symmetrical about a mirror plane
dome
47
pair of faces symmetrical about an axis of rotation
sphenoid
48
proportional lengths of the 3 crystallographic axes
axial ratio
49
also called unit face any face that intersects all 3 axes at distances from the center that correspond to the axial ration of the mineral
unit plane
50
method describing the relationship between sets of crystal faces or planes and the crystallographic axes that are always expressed in the sequence a b c where each represents their respective axes generally k k l where each represent a b and c axis
weiss parameters
51
the reciprocal of any faces or set of planes weiss parameters written as hkl that represents the reciprocal of the face of the planes of the weiss parameters of the a b and c axis respectively
miller indices
52
what are the forms under isometric
cube 001 6 square faces halite galena pyrite fluorite octahedron 111 8 triangular faces spinel magnetite chromite diamond dodecahedron 011 12 diamond shaped faces garnet sphalerite sodalite cuprite tetrahedron 111 4 triangular faces tetrahedrite sphalerite pyritohedron h0I 12 pentagonal faces pyrite
53
forms under tetragonal
tetragonal dipyramid 111 hh1 011 8 triangular faces with top 4 separated from bottom 4 by mirror plane zircon rutile cassiterite wolfenite tetragonal prism 0kl and variations 4 rectangular faces parallel to c axis scheelite vesuvianite malachite azurite tetragonal disphenoid 0kl 4 triangular faces with alternation pairs symmetrical about c axis chalcopyrite basal pinacoid 001 pair of faces perpendicular to c axis vesuvianite wolfenite
54
forms under hexagonal
hexagonal dipyramidal 1121 12 triangular faces inclined to c axis with top 6 separated from bottom 6 by mirror plane apatite zincite hexagonal prism 1120 6 rectangular faces parallel to c axis apatite quartz tourmaline basal pinacoid 0001 pair of faces perpendicular to c axis beryl corundum
55
forms under trigonal?
rhombohedron 6 parallelogram faces inclined to c axis dolomite siderite rhodochrosite trigonal scalenohedron 23 scalene triangle faces inclined to c axis calcite trigonal prism 3 rectangular facs parallel to c axis tourmaline quartz calcite trigonal dipyramid 6 triangular faces top 3 separated from bottom 3 by a mirror plane tourmaline
56
orthorhombic forms?
rhombic pyramids 8 triangular faces top 4 separated from bottom 4 by a mirror plane topaz aragonite olivine rhombic pyramids 4 rectangular faces parallel to a single crystallographic axis stibnite celestite enstatite pinacoids 2 parallel faces perpendicular to a b or c axis andalusite hemimorphite barite
57
monoclinic forms?
monoclinic prisms 4 rectangular faces gypsum staurolite clinopyroxene pinacoids 001 010 110 pair to rectangular perpendicular to a b c axis sphene epidote micas
58
triclinic forms?
pinacoids 2 parallel faces kyanite plagioclase microcline pedions single face rhodonite wollastonite
59
what is the weight of a nucleus and protons
1.00867 amu nucleus 1.00728 amu protons
60
who developed the periodic table of elements
dmitri mendeleev march 1 1869
61
the amount of energy required to strip an element of an electron from its outermost shell
ionization potential
62
mineral groups that has no group or subgroup?
antimonides sb^3 arsenates asO4^3 arsenides As^3 borates BO3^3 BO4^-3 chromates CrO4^-2 molybdates MoO4^-2 nitrates NO3^-1 phosphates PO4^-2 selenides Se^-2 sulfides S-2 tellurides Te-2 Tungstates WO4^-2 Vanadates VO4^-2
63
what are the mineral groups of carbonates?
calcite group CO3^-2 dolomite group aragonite group
64
groups under the mineral group halides
anhydrous halides hydrous halides CL-1 Br1 F1
65
what are the subgroups under hydroxides?
brucite type group gibbsite type group OH1
66
what are the groups under native element
metals group: gold group platinum group iron group semimetals group non metals group
67
groups under oxides?
simple oxides group: protoxide subgroup XO-2, X2O-2 rutile subgroup XO2^-2 hematite group X2O3^-2 complex oxides group: spinel group XY2O4^-2 iron subgroup chromite subgroup O-2
68
groups under silicates?
nesosilicates island silicates 1:4: olivine garnet aluminum silicates group SiO4^-4 sorosilicates double island silicates 2:7: Epidote group Si2O7^-6 cyclosilicates ring silicates- 1:3: beryl tourmaline group Si2O7^-6 inosilicates chain silicates - 1:3: pyroxene single Si2O6^-4 amphibole double silicate Si4O11^-6 phyllosilicates sheet silicates 2:5: mica group serpentine clay chlorite Si2O5^-2 tectosilicates framework silicates 1:2: silica feldspathoid plagioclase feldspar potassium feldspar group scapolite zeolite SiO2
69
groups under sulfates?
anhydrous sulfates hydrous sulfates SO4^-2
70
this theory suggests that beams of light consist of material particles that spread in all directions from luminous bodies
corpuscular theory
71
particle of lights which are discrete packets of energy that interact with atoms at the subatomic level
photons
72
assumes that units of quanta radiates discontinuously from radiating oscillators in a black body
quantum theory
73
surface that represents the direction of the propagation of light energy simultaneously in same place
wavefront
74
line at any point in the direction of the propagation of light perpendicular to the surface of a wave front
wave normal
75
perpendicular to the wavefront represents the direction of propagation of light
ray of light
76
materials whose light passing through them have light rays parallel to the wave normal and perpendicular to the wavefront
isotropic
77
light passing have light rays that are not parallel to the wave normal
anisotropic
78
curve that may represent that combined movement around a circle with movement along a straight line
displacement
79
component of light found on the wavefront that is perpendicular to the light ray in isotropic materials but is only perpendicular in limited directions for anistropic materials
vibration direction
80
filters the light and eliminate the orange light
base blue filter
81
polarizes light in a single wave direction generally only those oriented in the N-S direction
sub stage polarizer (lower polarizer)
82
controls the amount of light passing through the specimen
sub stage iris diaphragm
83
controls and focuses the light from the light source
sub stage condenser
84
used to retard the light coming through the specimen
intermediate accessory plates
85
polarizes light in a single wave direction only those in the E-W direction
intermediate analyzer (upper polarizer)
86
used to observe interference figures
intermediate bertrand lens
87
magnifies the observed image
intermediate objective lens
88
adjusts the stage's distance from the objective lens
stand coarse adjustment knob
89
focuses and sharpens observed image
stand fine adjustment knob
90
let's users to observe the image produced
Assembly: Ocular Part: Eyepiece
91
ratio of the wave normal velocity in a vacuum regardless if the medium is isotropic or anisotropic
refractive index
92
light consists of a single wavelength
monochromatic light
93
component of light vector that lies parallel to the wave front and perpendicular to the direction of the propagation except for anisotropic minerals
light vector
94
light vector that measures the electrical displacement
electric light vector
95
measures magnetic displacement
magnetic light vector
96
147nm retardation dimensions are usually NW-SE
mica plate
97
550nm retardation dimensions are usually NW-SE
gypsum plate
98
various retardation to determine the order of the interference color exhibited by a mineral
quartz wedge
99
optically positive if the interference color between the melatope ; negative if melatope
decreases; increases
100
optically positive if the colors move in along the trace of the OAP and out along the ON
negative if the colors MOVE OUT along the trace of the OAP and in along the ON
101
monoclinic variety of albite
monalbite
102
lapiz lazuli, chalcedony amazonite and jasper were cut and curved where?
babylonia
103
it is also known an emerald filter
chelsea
104
also called flame fusion, was the first commercially successful method of manufacturing synthetic gemstones, developed in the late 1883
Verneuil method
105
also called as crystal pulling
Czochralski process
106
heavy walled steel cylinder closed at one end
autoclave or bomb
107
a process for growing single crystal or crystals of a metal or compounds. ruby and emerald are grown here
Flux method
107
which materials dyeing used
chalcedony jade and turquoise
107
gems successful for heat treatment
zircon quartz beryl topaz and zoisite (tansanite)
108
clinonet is also known as what?
clinonet
109
what is called as german silver?
iron nickel zinc
110
equation describing the relationship of than angle of incidence and angle of refraction with the refractive index of the light in air and in the medium and predicts that incident light that is not perpendicular to the surface of the medium will always be refracted in the medium
snells law
111
degree of visibility of a transparent mineral in an immersion medium or the difference between the refractive index between a mineral and a medium
relief
112
difference between RI of the mineral and the surrounding medium that involves a halo around the boundary of the mineral grain, and becomes either less or more visible as you increase the free working distance by defocusing the microscope
becke line method
113
difference between the RI of the mineral and the surrounding medium that involves blocking parts of the light and observing the shadow of the mineral grain. The RI of the mineral is higher than the surrounding medium if the shadow is on the lighted part of the visible field while it is lower when its shadow is on the darkened part of the visible field
oblique illumination method
114
composed of two rays
cross polarized light
115
travels in the low refractive index direction
fast ray
116
travels in high refractive index
slow ray
117
measured in number of wavelengths and it is the amount by which the slow rays lag behind the fast ray. It is proportional to the birefringence and to the distance traveled through the specimen
retardation
118
twinning where two crystals form as penetration twins
carlsbad twinning
119
lamellae are both observed with respect to each other and every alternate twin plate or slab has an identical atomic structure
lamellar twinning
120
two kinds of repeated twinning in thin sections with one set of twins arranged at 90 to other set
tartan twinning
121
outer rim is composed of low temp mineral compared to its center which is composed of high temp mineral of the same solid solution
normal zoning
122
outer rim is composed of high temperature mineral compared to its center which is composed of low tem mineral of the same solid solution
reverse zoning
123
step like progression of higher temp mineral tot he lower temp mineral at margins with local reversals in adjacent zones
oscillatory zoning
124
minerals extinct at certain angles that may be due to being deformed
undulatory extinction
125
systematic pattern of chemical variations from solid solution which starts at the periphery of the crystal towards the center regarding an incomplete continuous chemical reaction between the crystal and surrounding melt
zoning
126
divisions in the michel levy chart for every 550um that is marked by a reddish hue interference color
order
127
lens inserted below the oculars used to observe interference figures
bertrand lens
128
bands of interference colors which increases in order form the melatope to the outer bands
isochrome
129
arms of the interference figure
isogyre
130
point where the isogyres cross and where the optic axis emerges
melatope
131
specific direction in anisotropic minerals where only one ray travels through the mineral
optic axis
132
is a sphere and indicatrix with constant radius due to light travelling in all directions with the same velocity
isotropic indicatrix
133
an ellipsoid that revolves around the crystals c axis optic axis
uniaxial indicatrix
134
anisotropic minerals where minerals with tetragonal and hexagonal crystal system belong which have only one optic axis
uniaxial minerals
135
semi axis perpendicular to the c axis that has length proportional to the RI perpendicular to c and is associated with the ordinary light
omega
136
one of the two rays refracted when light entered uniaxial minerals and always moves parallel to the c axis which is parallel tot he crystals c axis and is always perpendicular to the extraordinary ray
ordinary ray
137
semi axis parallel to the c axis that has a length proportional to the RI parallel to c and is associated with the extraordinary ray
epsilon
138
one o fthe two rays refracted when light entered uniaxial minerals and moves anywhere between perpendicular to nearly parallel to the ordinary wave and is always perpendicular to the ordinary ray
extraordinary ray
139
intermediated refractive indices possessed by intermediate velocities of epsilon that are associated with other e ray directions
epsilon prime
140
perpendicular to the optic axis the c axis and ordinary ray path
circular section
141
viewed when the optic axis is parallel to the stage which is parallel to the extraordinary wave vibration direction
principal section
142
other section parallel to the stage that have two rays pass through the crystal path ans is associated with epsilon prime
random sections
143
a sign that denotes ray is associated with either the larger or smaller refractive index
optic sign
144
uniaxial minerals that are geometrically prolate that occurs when the epsilon which is the slow ray and associated with the larger refractive index and is more than the omega whish is the fast ray associated with the smaller refractive index
uniaxial positive
145
uniaxial minerals that are geometrically prolate that occurs when the epsilon which is the slow ray and associated with the larger refractive index and is lesser than the omega whish is the fast ray associated with the smaller refractive index
uniaxial negative
146
an accessory plate used for minerals with low birefringe in order to determine their optic sign by retarding the ineral by 550um or specifically one order
gypsum plate
147
observed when the optic axis is perpendicular to the stage so that the circular section is parallel to the stage
centered uniaxial optic axis OA figure
148
observed when the optic axis is inclined more steeply than 60 - 70 degrees with respect tot he stage making a random section parallel to the stage
off centered optic axis OA figure
149
observed when the optic axis lies within the plane of the stage making a principal section being viewed thus both the omega and epsilon vibration directions being observed. The flash figure will be observed every 90 degrees rotation of the stage when the optic axis is parallel to one of the two polarizing lenses
uniaxial flash figure
150
a triaxial ellipsoid the represents the refractive indices of a biaxial mineral in every direction
biaxial indicatrix
151
class of anisotropic minerals where minerals are triclinic monoclinic and orthorhombic crystals systems belong which have only two optic axes
biaxial minerals
152
minimum refractive index in the biaxial indicatrix that is associated with the short axis of the ellipsoid X parallel to the vibration direction of the fast ray
alpha
153
minimum refractive index in the biaxial indicatrix that is associated with the long axis of the ellipsoid Z parallel to the vibration direction of the slow ray
gemma
154
intermediate refractive index in the biaxial indicatrix that is associated with the intermediate axis of the ellipsoid Y associated with the vibration direction of an intermediate ray
beta
155
elliptical XY plane
optic plane
156
elliptical XZ plane perpendicular to the Y
157
elliptical XZ plane perpendicular to the Y
optic axial plane
157
circular sections in a biaxial indicatrix that are perpendicular to the two sections
optic normal sections
157
the angle between the optic axes measured in optic plane
optic angle 2V
158
line parallel to the y axis of a biaxial indicatrix that intersects the optic normal sections
optic normal
159
line in the optic plane that bisects the optic angle between the optic axes
optic normal
160
complementary line that bisects the optic angle that may either 2Vx or 2Vz depending on the mineral optics
acute bisectrix bxa
161
accessory plate used for minerals with high birefringence to easily determine their optic signs
quartz wedge
162
biochemical sedimentary rocks that contain more than 15% by weight and occur in rocks that range in age from 3.8 Ga to the present
iron rich bichemical sedimentary rocks
163
constitutes 60% of the iron ores
banded iron formation
164
type of BIf dominate the archean iron rich sedimentary rocks that formed between 3.8 ga and 2. 6 ga
algoma type BIF
165
dominate the proterozoic iron rich sedimentary rocks the formed between 2.6 GA and 1.8 Ga and again 0.8 Ga to 0.5 Ga and are supposedly much larger compared to algoma type
superior type BIF
166
iron formation contained superior type of BIF which formed in fairly shallow water environments on passive continental shelves with limited influx of detrital sediments
granular iron formation
167
most widespread type of phanerozoic iron rich sedimentary rock that are quite thin and are composed predominantly of goethite and hematite with smaller amounts of iron bearing chlorite mineral chamosite
ironstone
168
contain less than 30% gravel sized clasts and sand mud ratio of <1:1 in their detrital fraction
mudrocks
169
smectite rich that formed from the alteration of volcanic as deposits from explosive eruptions
bentonite
170
at what temp and pressure does diagenesis occur?
~150 +- 50 degrees celcius and ~0.3 kbar
171
early shallow diagenesis that occurs shortly after burial
eodiagenesis
172
later deeper diagenesis
mesodiagenesis
173
even later and shallow diagenesis that occurs as sedimentary rocks approach the surface due to erosion
telodiagenesis
174
diagenetic product of plastic grains that can be difficult to distinguish from detrital matrix constituents
pseudomatrix
175
most abundant group of biochemical sedimentary rocks and constitute about 15% of all sed rocks
carbonates
176
also called as allochems sand to gravel sized carbonate particles that include shells ooids and limeclasts and peloids
grains
177
also called as allochems sand to gravel sized carbonate particles that include shells ooids and limeclasts and peloids
grains
178
mud sized carbonate particles in limestones and dolostones
micrite
179
process where micro boring activity of blue green cyanophyt texture
micritization
180
emphasizes the texture of carbonate rocks
dunham classification
181
emphasizes thecomponents of carbonate rocks
folks classification
182
carbonate rocks with gravel sized particles
calcirudite/dolorudite
183
carbonate rocks with sand sized particles
calcarenite/dolarenite
184
carbonate rocks with mud sized particles
calcilutite/dololutite
185
composed of lithified colluvium deposited from mass wasting
diamictite
186
less than 30% gravel sized clasts and a sand:mud ratio of >1:1 in their detrital fraction
sandstones
187
sandstones containing 75-95% quartz grains with F:L ratio 1:>1
subarkose
188
sandstones containing 75-95% quartz grains with F:L ratio of 1:> 1
sublitharenite
189
rock fragment rich sandstones
lithearenite
190
contains less than 75% quartz grains with F:L ratio between 1:1 to 3:1
lithic arkose
191
contains less than 75% quartz grains with F:K ratio between 1:1 to 1:3
feldspathic litharenite
192
how many percent is sed rocks in earths surface
85%
193
quick method of determining the phi size value for any percentile
sorting coefficient
194
more complicated measure of sorting that involves finding values that are one standard deviation and two standard deviations above and below the mean
inclusive graphic standard deviation
195
rod shaped particles that have an elongate cylindrical that have on axis much longer than the other two
prolate
196
disk shaped particles that have a flattened cylindrical or disk like shape where two saxes are shorter than the other two
oblate
197
particles that have a flattened shape where the 3 axes have 3 different lengths
bladed
198
gravelstones with an interior source eroding from the same source and lithifying in place making the clasts and matrices compositions uniform
intraformational
199
compositions derived outside of depostional basin with the clasts and matrices composition different from each other
extraformational
200
more than 90% of the framework clasts consisting of a single or few resistant rocks and minerals
oligomict
201
clasts of different compositions that are prone to weathering and erosion
petromict
202
clasts composed of a single composition
monomictic
203
2-4 different types of parent rocks
diamictic
204
clasts with numerous amounts of types of composition
polymictic
205
the total overall retardation is greater than that exhibited prior to the accessory plate being inserted
positive elongation
206
what are the isotropic minerals with low relief
halite halloysite antigorite cliachite collophane
207
what are the isotropic minerals with moderate relief
opal fluorite lechatelierite sodalite analcime hauyne
208
what are the isotropic minerals with moderate to strong relief
periclase garnet group grossularite pyrope almandite spessarite uvavorite andradite
209
what are the isotropic minerals with very high relief
limonite spinel chromite perovskite sphalerite
210
do not affect the polarization direction of the light which has passed through lower polarizer
isotropic minerals
211
will appear dark or extinct every 90 degrees of rotation of the microscope stage
anisotropic minerals
212
produce elongate grains and cleavage are distinguishable
biotite hornblende plag
213
production of plane polarized refractive index
nicol prism
214
minerals that exhibit parallel extinction
orthopyroxene biotite
215
minerals that exhibit inclined extinction
clinopyroxene hornblende
216
minerals that exhibit symmetrical extinction
amphibole calcite
217
minerals that exhibit no cleavage
quartz olivine
218
measures double refraction
snells law
219
how many known minerals
4000 but 50 are common
220
refractive index varies inversely with wavelength snells law
dispersion of light
221
cleavage exhibits 56- 124 degrees
amphibole group
222
two segments of one grain go extinct at different times as the stage is rotated
simple twins
223
the segments are joined by a smooth twin plane separating the segments
contact twins
224
the segments are joined by an irregular contact
penetration twins
225
consists of numerous twin segments joined on parallel twin planes
polysynthetic twinning
226
the separation of a single homogeneous mineral into two or more distinct minerals in the solid state
exsolution or unmixing ex: perthite albite exsolution from orthoclase at about 56 degrees celsius
227
successive layers of sheet structure show regular variations in their orientation occurs in micas and clay
polytypism
228
this mineral is colorless not pleochroic anhedral no cleavage very low relied uniaxial and length is slow
quartz
229
colorless but cloudy not pleochroic subhedral to anhedral 2 cleavage directions low relief biaxial carlsbad and tartan twinning
alkali feldspars
230
colorless no pleochroic euhedral to anhedral perfect cleavage directions low relief weak birefringence polysynthetic albite carlsbad pericline twinning triclinic feldspars
plag felds
231
An0 to An10
albite
232
an90- an100
anorthite
233
intergrowth where soda rich phase predominates over potash rich phase
antiperthite
234
their atomic ration exceeds that of alkali feldspars
feldspathoids nepheline sodalite leucite
235
colorless not pleochroic high relief no to poor cleavage strong birefringence parallel extinction length slow
olivine
236
F065-FO0
fe rich igneous rock
237
colorless and weakly pleochroic 2 cleavage directions at 87 and 93 degrees stubby crystals bery high relief weak to moderate birefringence parallel inclined symmetric extinctions
pyroxenes
238
orthorhombic orthopyroxenes
enstatite bronzite hypersthene ferrosilite
239
monoclinic ca mg fe pyroxenes
augite pigeonite diopside hedenbergite
240
sodic pyroxenes
aegerine-jadeite
241
colored with varying pleochroism slender crystals high relief 2 cleavage directions mod to strong birefringence parallel inclined symmetric
amphibole
242
mg fe amphiboles
antophyllite-cummingtonite-grunerite
243
ca fe mg amphiboles
tremolite-actinolite-hornblende
244
sodic amphiboles
glaucophane-ribeckite-arvedsonite
245
various shades of brown with tinges of red and green highly pleochroic 1 perfect basal cleavage fair relief strong birefringenece high interference color parallel inclinced biaxial
biotite
246
minute crystals usually tabular or prismatic habit and birefringent
microllites
247
smaller spherical rod like and hair like isotropic forms
crystallites
248
an aphanitic or glassy texture that are completely free of phenocrysts
aphyric
249
some are euhedral subhedral rest are anhedral
granitic structure
250
all are anhedral
aplitic texture
251
phenocrysts are gathered distinct clusters
glomeroporphyritic
252
monomineralic clusters in a glomeroporphyritic texture
glomerocrysts
253
polyminerallic clusters in a glomeroporphyritic texture
cumulocrysts
254
continuous ranges of size in crystals of the principal minerals in a fine grained matrix
seriate
255
broken series of sizes
hiatal
256
relatively large crystal of one mineral (oikocryst) enclose numerous smaller crystals of one or more other mineral (chadacryst) which are randomly oriented oikocryst is the latest to finish crystallizing
poikolitic
257
randomly arranged plagioclase chadacrysts are elongate and ate wholly poikolophitic enclosed by the augite oikocryst
ophitic
258
glass occupies wedge shaped interstices between plan laths
intersertal
259
spaces between plag laths are occupied by one or more grains of pyroxene olivine or opaque minerals
intergranular
260
other term for euhedral
idiomorphic automorphic
261
other term for subhedral
hypidiomorphic hypoautomorphic
262
other term for anhedral
xenomorphic allotriomorphic
263
subparallel arrangement of microcystalline lath shaped feldspars in groundmass
trachytic
264
trachytic texture with crystalline material in between feldspars
pilotaxitic
265
trachytic texture with cglassy material in between feldspars
hyalopilitic
266
subparallel arrangement of tabular bladed or prismatic crystals which are visible to the naked eye
trachitoid
267
dense holocrystalline tightly appressed microlites generally of feldspars interwoven in irregular unoriented fashion
felty
268
boundary involves interdigitations
consertal
269
form a eutectic mixture or through replacements similar to cuneiform writing
graphic
270
patches of plag felds intergrown with vermicular qtz
mermyktic texture
271
intimate intergrowth of 2 minerals in which one mineral has a vermicular
symplectite texture
272
composed of an aggregate of fibtrous crystals radiating from a nucleus with glass or crystals in between
spherulitic
273
radiate texture with radiating fibers extending from either end if linear nucleus rahter than a point
axiolitic
274
radiate texture with fanlike arrangement of divergent often branching fibers
variolitic
275
crystal of one mineral is surrounded by a rim or mantle of one or more crystals of another mineral
corona
276
corona texture charac by an overgrowth by NA plag on large K felds
rapakivi
277
charac by an overgrowth of pyroxene of hornblende or olivine or garnet
kelyphitic
278
one or more concentric bands ina single crystal are picked out by lines of inclusions or by gradual or abrupt changes in solid solution
zoning
279
charac having dips or bay like section in thte crystals as a result of resorption disequilibrium
embayed
280
how many space groups are determined?
230 space groups
281
4-faced form where the faces are related by mirror planes
Rhombic Pyramid
282
4-faced form where the faces are related by a 4 axis
Tetragonal Pyramid
283
8-faced form where all faces are related by a 4 axis.
Ditetragonal Pyramid
284
o 12-faced form where all faces are related by a 6-fold axis. This form results from mirror planes that are parallel to the 6-fold axis
Dihexagonal Pyramid
285
are closed forms consisting of 6, 8, 12, 16, or 24 faces. Dipyramids are pyramids that are reflected across a mirror plane. Thus, they occur in crystal classes that have a mirror plane perpendicular to a rotation or rotoinversion axis
Dipyrami
286
are closed 6, 8, or 12 faced forms, with 3, 4, or 6 upper faces offset from 3, 4, or 6 lower faces.
Trapezohedrons
287
closed form with 8 or 12 faces. In ideally developed faces each of the faces is a scalene triangle. In the model, note the presence of the 3-fold rotoinversion axis perpendicular to the 3 2- fold axes
Scalenohedrons
288
6-faced closed form wherein 3 faces on top are offset by 3 identical upside down faces on the bottom, as a result of a 3-fold rotoinversion axis.
Rhombohedrons
289
closed form consisting of 4 faces. These are only present in the orthorhombic system (class 222) and the tetragonal system (class )
Disphenoids
290
A hexahedron is the same as a cube. 3-fold axes are perpendicular to the face of the cube, and four axes run through the corners of the cube.
Hexahedron
291
8 faced form that results form three 4-fold axes with perpendicular mirror planes. The octahedron has the form symbol {111}and consists of the following 8 faces: (111), (), (11), (1), (1), (1), (11), and (11).
Octahedron
292
12-faced form. Dodecahedrons can be formed by cutting off the edges of a cube. The form symbol for a dodecahedron is {110}.
Dodecahedron
293
12-faced closed form with the general form symbol {hhl}. This means that all faces intersect two of the a-axes at equal length and intersect the third a-axis at a different length
Trapezohedron
294
occur as accessory minerals in igneous and metamorphic rocks and as resistant detrital grains in sediments
Oxides
295
Includes the majority of ore minerals
Sulfides
296
adjacent silica tetrahedra share oxygens to form the different types of silicates
polymerization
297
describes the phenomena of polarization, reflection, refraction and interference, which form the basis for optical mineralogy
Wave theory
298
In isotropic materials the Wave Normal and Light Ray are?
parallel
299
A measure of how effective a material is in bending light is called
Index of Refraction (n)
300
used to calculate how much the light will bend on travelling into the new medium
Snell's law
301
in which minerals are seen with pleochroism?
tourmaline, biotite, hornblende, (most amphiboles), some pyroxenes.
302
The ability to selectively transmit and absorb light is termed
pleochroism
303
involves the determination of the refractive index of minerals, using the immersion method.
Refractometry
304
This method relies on having immersion oils of known refractive index and comparing the unknown mineral to the oil.
Refractometry
305
the degree to which a mineral grain or grains appear to stand out from the mounting material, whether it is an immersion oil, Canada balsam or another mineral
Relief
306
the indices of the mineral and surrounding medium differ by greater than 0.12 RI units.
Strong relief
307
indices differ by 0.04 to 0.12 RI units
Moderate relief
308
Indices differ by or are within 0.04 RI units of each other
Low relief
309
what is the index of oil
1.45
310
It is a band or rim of light visible along the grain boundary in plane light when the grain mount is slightly out of focus.
Becke Line
311
exhibits parallel extinction inclined symmetrical
orthopyroxene biotite Clinopyroxene, Hornblende amphibole; calcite
312
become familiar with this plate, it produces ~550 nm of retardation. The interference colour in white light is a distinct magenta colour. This colour is found at the boundary between first and second order colours on Plate 1. First Order Red Plate)
Gypsum Plate
313
Retardation of 147 nm, the interference colour is a first order white
Mica Plate
314
Wedge shaped and produces a range of retardations
Quartz sWedge
315
the overall total retardation is less than that exhibited by the mineral prior to the accessory plate being inserted.
negative elongation
316
the total overall retardation is greater than that exhibited prior to the accessory plate being inserted
- POSITIVE ELONGATION,
317
Minerals which display moderate to strong birefringence may display a change in relief as the stage is rotated, in plane light.
Relief
318
coloured anisotropic minerals display a change in colour
pleochroism or diachroism
319
form when the vibration directions in the interference figure parallel the vibration directions of the polars. These are areas of extinction
Isogyres
320
breaking up of the white light
Dispersion
321
Plane-Polarized (PPL) Properties
Color - Pleochroism - Habit - Cleavage and Fracture - Relief - Index of Refraction
322
Cross-Polarized (XPL) Properties
Birefrringence - Extinction - Sign of Elongation - Twinning and Zoning
323
This property is present when areas with differing extinction orientations within the same mineral grain have planar contacts.
Twinning
324
polarizing transmitted-light microscope, commonly known as
petrographic microscope
325
typical bulb used has a tungsten filament, which gives the field view a yellowish tint.
The Light Source
326
used to reduce the area of light entering the thin section and should be in focus at the same position asthe thin section: it should be opened until it just disappears
field diaphragm
327
closed to increase resolution, it can be seen when the Bertrand’s lens is inserted
aperture diaphragm
328
serves to direct a cone of light on the thin section and give optimum resolution for the objectives used small circular lens (the condenser) is attached to a swivel bar, so that it can be inserted into the optical train when required
Condenser and Convergent Lens
329
marked in degree units and a side vernier enables angles of rotation to be accurately measured
Stage
330
power of magnification inscribed on each lens (e.g. x5, x30). An objective of very high power (e.g. x100) usually requires immersion oil between the objective lens and the thin section
Objectives
331
used to examine interference figures. When it is inserted into the upper microscope tube an interference figure can be produced which fills the field of view, provided that the convergent lens (condenser) is also inserted into the optical path train
The Bertrand Lens
332
The slot is oriented so that accessory plates are inserted at 45o to the cross wires. In some microscopes the slot may be rotatable
The Accessory Slot
333
what is the grit called
carborundum grit
334
standard thickness
30 microns
335
30 microns
Buffing
336
> 66 wt. %
Felsic
337
52 – 66 wt. % SILICA
Intermediate
338
45 – 52 wt. % silica
Mafic
339
silica content < 45 wt. %
Ultramafic
340
usually occur from the rapid crystallization of lava extrusive rocks cool very quickly, therefore their minerals form fine crystals which cannot be seen and distinguished by the naked eye
Aphanitic
341
type of texture id formed when magma cools and some minerals increase in size extensively. The sizes may range from some centimeters to quite a number of meters
Pegmatitic
342
plutonic igneous rocks, which underwent slow crystallization underneath the surface of the earth
Phaneritic
343
can also form when magma is crystallized under a volcano but eruption occurs before the crystallization is complete.
porphyritic texture
344
low silica and gas contents make them very fluid; i.e., they have a low viscosity, or resistance to flow
Classification of Ultramafic Intrusive Rocks Classification of Pyroclastic Rocks Ultramafic Rocks
345
intrusive ultramafic rocks,
peridotite
346
extrusive ultramafic rocks.
komatiite
347
Rocks composed mostly of pyroxene, calcium-rich plagioclase, and minor amounts of olivine
Mafic Rocks
348
Rocks composed mostly of hornblende and intermediate plagioclase feldspars produced primarily in convergent plate boundaries in which an oceanic plate is subducting beneath either another oceanic plate a continental plate
Intermediate Rocks
349
similar to pumice but usually made of iron rich minerals found in basalt lava
cinders (scoria)
350
mafic crystals of felsic intermediate mafic ultramafic
1-15% 16-45% 46-85% >85%
351
occurs between diagenesis and melting
Metamorphism
352
rock or metamorphic formation which has arrived at a chemical equilibrium through metamorphism at constant temperature and pressure conditions, the mineral composition is controlled only by the chemical composition
metamorphic facies
353
substantial chemical change accompanies metamorphism involves the infiltration of fluids and/or the diffusion of material through the fluid and solid phases chemical alteration takes place as a result of these fluids
Metasomatism
354
when the T-P increases on a body of rock
Prograde metamorphism
355
T-P fall due to erosion of overlying rock or due to tectonic uplift
Retrograde metamorphism
356
Pressure increases with depth due to the weight of the overlying bedrocks
lithostatic pressure
357
orce acting equally from all directions, it is a type of stress called hydrostatic stress, or uniform stress.
Pressure
358
rocks undergo metamorphic reactions due to heating (little or no pressure change) when a hot igneous intrusion (magma) comes into contact with cold country rock, it creates a metamorphic aureole / contact aureole or baked zone. produces hornfels, a nonfoliated metamorphic rock
Contact Metamorphism
359
Rock in the deep portions of faults undergoes dynamic metamorphism and creates a fine grained metamorphic rock called
mylonite
360
referred to as shock quartz
coesite or stishovite
361
Started out originally with clay minerals and as a result of metamorphism, alumna rich minerals form
Pelitic
362
The clay minerals have recrystallized into tiny micas which reflect a glossy luster
Phyllite
363
The rock developed a near planar foliation caused by the preferred orientation of sheet silicates. However, quartz and feldspar grains show no preferred orientation
Schist
364
irregular planar foliation
schistosity
365
When non-mica minerals (quartz, feldspars, kyanite, garnet, staurolite, and sillimanite) occur with a grain size greater than the rest of the rock, they are called
pophyroblasts
366
dark colored minerals tend to become segregated in distinct bands through the rock, giving the rock
gneissic banding
367
e highest grades of metamorphism, all of the hydrous minerals and sheet silicates become unstable and thus there are few minerals present that would show this
granulite
368
the temperature reaches the solidus temperature, the rock may begin to melt and start to comingle with the solids. Usually these solids are felsic with the mafic material remaining metamorphic
Migmatites
369
Usually poorly foliated and form at intermediate to high grades of metamorphism of basaltic or gabbroic protoliths
Amphibolite
370
Very fine- grained rocks that usually form as a result from magma intruding into fine grained igneous rocks or shales. - The magma causes a type of metamorphism called contact metamorphism.
Hornfels
371
Mineral assemblages form from fine-grained unstable starting materials such as glassy volcanic rocks, pyroclastics and greywackes. Diagnostic minerals may also occur in veins cutting largely unrecrystallized rocks
Zeolite Facies and Prehnite-Pumpellyite Facies
372
what are the Intermediate Pressure Facies
Zeolite Facies and Prehnite-Pumpellyite Facies Greenschist facies Amphibolite facie Granulite facies
373
heulandite + analcite + Qtz ± clay minerals * laumontite + Ab + Qtz ± Chl * prehnite + pumpellyite + Chl + Ab + Qtz * pumpellyite + Chl + Ep + Ab + Qtz * pumpellyite + Ep + stilpnomelane + Musc + Ab + Qtz
Metavolcanics and greywackes
374
Musc + Chl + Ab + Qtz (indistinguishable from greenschist facies)
Metapelitic rocks
375
Chl + Ab + Ep ± actinolite, Qtz * Metagreywackes * Ab + Qtz + Ep + Musc ± stilpnomelane * Metapelites * Musc + Chl + Ab + Qtz * chloritoid + Chl + Musc + Qtz ± paragonite Bt + Musc + Chl + Ab + Qtz + Mn-rich garnet
Metabasic rocks (Greenschist facies)
376
* Dolomite + Qtz
Siliceous dolomites (Greenschist facies)
377
Hbl + Pl ± Ep, garnet, cummingtonite, diopside, Bt
Metabasic rocks (Amphibolite facies)
378
Musc + Bt + Qtz + Pl ± garnet, staurolite, kyanite/sillimanite * Siliceous dolomites * dolomite + calcite + tremolite ± talc (lower amph. f.) * dolomite + calcite + diopside and/or Fo (upper amph. f.)
Metapelitic rocks (Amphibolite facies)
379
Forms under conditions of P(H2O)
Granulite facies
380
Opx + Cpx + Hbl + Pl ± Bt * Opx + Cpx + Pl ± Qtz * Cpx + Pl + garnet ± Opx (higher P) * Metapelitic rocks * garnet + cordierite + sillimanite + K-feldspar + Qtz ± Bt * sapphirine + Opx + K-feldspar + Qtz ± osumilite (very high T)
Metabasic rocks (Granulite facies)
381
what are the High Pressure Facies
Blueschist Facies. Eclogite Facies
382
Known also as the glaucophane-lawsonite schist facies; these occur along Mesozoic and Tertiary orogenic belts such as the circum-Pacific belts and the Alpine-Himalayan chain. In high pressure rocks, mica is phengite rather than muscovite.
Blueschist Facies
383
glaucophane + Law + Chl ± phengite/paragonite, omphacite * Metagreywackes * Qtz + jadeite + lawsonite ± phengite, glaucophane, Chl
Metabasic rocks (Blueschist Facies )
384
phengite + paragonite + carpholite + Chl + Qtz
Metapelites (Blueschist Facies)
385
Aragonite
Carbonate rocks (Blueschist Facies)
386
Eclogitessensustricto are metabasic rocks, occurring in a variety of associations, e.g. as enclaves or tectonically-incorporated blocks in blueschists or medium to high grade gneisses, or as nodules brought up in kimberlite pipes. In certain regions, rocks preserve (albeit imperfectly) distinctive high-pressure assemblages. Plagioclase is entirely absent
Eclogite Facies
387
omphacite + garnet ± kyanite, Qtz, Hbl, zoisite
Metabasic rocks (eclogite facies)
388
Qtz + phengite + jadeite/omphacite + garnet
Meta-granodiorite (eclogite facies)
389
phengite + garnet + kyanite + chloritoid (Mg-rich) + Qtz * phengite + kyanite + talc + Qtz ± jadeite
Metapelites (eclogite facies)
390
what are the Low Pressure Facies
Albite-Epidote Hornfels Facies Hornblende Hornfels Facies Pyroxene Hornfels Facies Sanidinite Facies
391
Likely to be recognized only in the outermost parts of thermal aureoles in country rocks originally of very low metamorphic grade. This is the lowpressure equivalent of the greenschist facies, and the assemblages are very similar.
Albite-Epidote Hornfels Facies
392
Ab + Ep + actinolite + Chl + Qtz * Metapelites * Musc + Bt + Chl + Qtz
Metabasic rocks (Albite-Epidote Hornfels Facies)
393
Low pressure equivalent of the amphibolites facies. The assemblages described below can also be found in regionally metamorphosed rocks belonging to the low pressure facies series
Hornblende Hornfels Facies
394
Hbl + Pl ± diopside, anthophyllite/cummingtonite, Qtz
Metabasic rocks Hornblende Hornfels Facies
395
Musc + Bt + andalusite + cordierite + Qtz + Pl
Metapelites Hornblende Hornfels Facies
396
cordierite + anthophyllite + Bt + Pl + Qtz
K2O-poor sediments or metavolcanics Hornblende Hornfels Facies
397
same as amphibolite facies
Siliceous dolomites Hornblende Hornfels Facies
398
Developed in the inner parts of high temperature thermal aureoles, such as those around large basic bodies. Assemblages similar to granulite facies, but can be developed at P(H2O) = Ptotal Hornblende is not stable.
Pyroxene Hornfels Facies
399
* Opx + Cpx + Pl ± Ol or Qtz
Metabasic rocks Pyroxene Hornfels Facies
400
* cordierite + Qtz + sillimanite + Kfeldspar (orthoclase) ± Bt * cordierite + Opx + Pl ± garnet, Sp
Metapelites Pyroxene Hornfels Facies
401
calcite + Fo ± diopside, periclase * diopside + grossularite + wollastonite ± vesuvianite
Calcareous rocks Pyroxene Hornfels Facies
402
Rarely found, as the extremely high temperatures required are only achieved at direct contacts with flowing basic magma, or in completely-immersed xenoliths
Sanidinite Facies
403
cordierite + mullite + sanidine + tridymite (often inverted to Qtz) + glass
Metapelitic rocks Sanidinite Facies
404
* wollastonite + An + diopside * monticellite + melilite ± calcite, diopside * alsotilleyite, spurrite, merwinite, larnite and other rare Ca- or CaMg silicate
Calcareous rocks Sanidinite Facies
405
showed that metamorphism of tuffs in NZ accompanied by substantial chemical changes due to circulating fluids, and that these fluids played an important role in the metamorphic minerals that were stable
Boles and Coombs
406
Mafic Assemblages at Low Grades
Zeolite and prehnite-pumpellyite facies
407
Mafic Assemblages of the Medium P/T Series
Greenschist, Amphibolite, and Granulite Facies
408
constitute the most common facies series of regional metamorphism
greenschist, amphibolites and granulite facies
409
classical Barrovian series of pelitic zones and the lower-pressure BuchanAbukuma series are variations on this trend
Mafic Assemblages of the Medium P/T Series
410
Metamorphism of mafic rocks first evident
greenschist facies, which correlates with the chlorite and biotite zones of associated pelitic rock
411
impart the green color form which the mafic rocks and facies get their name
Chlorite, actinolite, and epidote
412
Amphibolite facies transition involves two major mineralogical changes 1. Albite→ oligoclase 2. Actinolite→ hornblende(amphibole accepts increasing aluminum and alkalis at higher T)
Greenschist
413
Mafic Assemblages of the Low P/T Series
Albite-Epidote Hornfels, Hornblende Hornfels, Pyroxene Hornfels, and Sanidinite Facies
414
Albite-epidote hornfels facies correlates with the greenschist facies into which it grades with increasing pressure
Hornblende hornfels facies correlates with the amphibolite facies, and the pyroxene hornfels and sanidinite facies correlate with the granulite facies
415
Mafic Assemblages of the High P/T Series The association of glaucophane + lawsonite is diagnostic
Blueschist and Eclogite Facies
416
characterized in metabasites by the presence of a sodic blue amphibole stable only at high pressures (notably glaucophane, but some solution of crosstie or riebeckite is possible)
blueschist facies
417
stable to lower pressures, and may extend into transitional zones
Crossite
418
breaks down at high pressure by reaction to jadeitic pyroxene + quartz:
Albite
419
Unstable minerals
pyroxenes, olivines, amphiboles, some plagioclase feldspars
420
Stable minerals
quartz, K-feldspar, Na- feldspar, muscovite, clay minerals, some 'heavy minerals'
421
(transported to the site of deposition
allogenic example: Framework grains and matrix
422
precipitated at the site of deposition
authigenic cements
423
Preferential orientation of particles in a sediment or tendency of a rock to break in specific directions
Fabric
424
cemented by minerals precipitated in pore spaces breccia and conglomerate
✓ Silica (quartz) ✓ Carbonate (calcite) ✓ Ferruginous (Fe-oxides)
425
Common cements
calcite, hematite, quartz, and clay
426
Common association on glacial till and debris flow deposits
Paraconglomerate
427
Flat-pebble conglomerates formed by mud rip-ups
Intraformational (within basin)
428
More likely to be petromictic
Extraformational (outside basin)
429
Three components of a rock:
Grains: > 0.03 mm (about φ5 = 31.3 mm; i.e. coarse silt and coarser). - Matrix: < 0.03 mm (finer than coarse silt); - Cement: not considered in this classification
430
high textural maturity, grain-supported fabric, grains held together by chemically precipitated cement.
< 15% matrix - arenites
431
15%-75% matrix
wackes: dirty, low textural maturity, largely matrixsupported fabric
432
The degree of mineralogical maturity can be determined by looking at the types of grains present
contains no feldspar (feldspar easily weathers to clay)
433
Presence of fresh, large, angular feldspar fragments in a sandstone imply
a high relief source area (rapid erosion, transport, burial, with little weathering effect OR ; b. a very arid or extremely cold climate (retards chemical weathering)
434
Small, rounded, highly weathered feldspars imply:
a. a low relief source area and/or warm, humid climate (modernintense weathering processe
435
Absence of feldspars imply
a. intense weathering (destroying feldspars) OR no feldspars in original source
436
rock fragments are chiefly of shale or slate
Phyllarenite
437
where the rock fragments are of limestone
Calcilithite
438
Feldspar is chiefly K feldspar and much of this is microcline. Texture is typically poorly- to wellsorted, with very typical red or pink, through the feldspar’s color, but also through the presence of finely disseminated hematite.
Arkoses
439
chiefly of mudrock and their low grade metamorphic equivalents and volcanic grains
Lithics
440
fluvial and deltaic sandstones Immature composition implies high rates of sediment production followed by short transport distances
Litharenites
441
fine-grained matrix, which consists of an intergrowth of chlorite, sericite and silt- sized grains of quartz and feldspar fine-grained sedimentary and meta-sedimentary rock types dominate. Feldspar grains are chiefly Na plag
Greywackes
442
oscillatory (microscale) zoning: volcanic or hypabyssal origin - progressive (coarse) zoning: igneous source, undifferentiated
Plagioclase Zoning
443
are the most abundant of all lithologies, some 45 - 55% of sed. rxs. - Main constituents - clays and qtz. - Clay mineralogy reflects to a greater extent the
MUDROCKS
444
calcareous mudrocks
Marls
445
<4µm; Silt - 4 to 62 µm
Clay -
446
usu. laminated and fissile.
Shale
447
used for a more indurated mudrock
Argillite
448
Absent when sediments are bioturbated, presence of much qtz silt or calcite, flocculation of clays during sedimentation
Fissility
449
mainly due to variations in grain size and/or changes in composition - Deposited in relatively short periods of time (hours or days) by turbidity currents or - Develops over months or years if there are annual or seasonal change in sediment supply or biological productivity
Lamination
450
The simplest phyllosilicates result from bonding one silicate layer to one octahedral layer. Because of this arrangement, we call these the 1:1 phyllosilicates
Phyllosilicate Structures
451
Montmorillonite and beidellite result from the alteration of volcanic ash to give bentonite clay deposits
Montmorillonite Group (Smectites) Clay Minerals
452
the most common clay mineral in sedimentary rocks
. Illite
453
Montmorillonite Group 2:1
Illite Chlorite
454
dominant in low-latitude areas, particularly off major rivers draining regions of tropical weathering. most important 1:1 phyllosilicate
Kaolinite
455
more common in ocean-floor muds of higher latitudes.
Illite
456
related to active mid-ocean ridge systems and volcanic oceanic islands
Smectites
457
25% of all sedimentary rocks ✓ Present from the pre-cambrian onward
Carbonate Rocks Pre-cambrian Carbonates – almost all dolomite - Tertiary Carbonates – very little dolomite
458
Carbonate Requirements
Sunlight – carbonates form in shallow water within the photic zone (0-60m); this is related to primary productivity (phytoplankton) 2. Turbidity – form in clear clastoic free water. Low turbidity enhances light penetration and prevents clogging of filter feeders, abrasion of shells by quartz 3. Temperature – form in warm water. Carbonate accumulate requires water below 20oC with consistent temperature 4. Stable normal oceanic salinity – 35 ppt 5. Thus, limited to within 30o Noth and South of equator (tropics and subtropics
459
Orthorhombic Crystal - Hardness of 4
Aragonite
460
Hexagonal (rhombohedral crystal) ▪ Hardness of 3
been dominant skeletal material in during the Paleozoic
461
Siderite – (FeCO3) * Magnesite – (MgCO3) * Rhodochrosite – (MnCO3)
Dolomite – CaMg(CO3)2
462
– fecal material excreted by benthic organisms
Peloids
463
These are exoskeletons or benthic (bottom-dwelling), mobile and sessile (esp. attached) organisms
Gastropods (Snails) * Pelecypods (Clams) * Echinoderms (Sand dollars, Starfish) * Cnidarians (Corals)
464
microgranular in many thinwalled foraminifera but fibrous in larger, thicker species, such as rotaliids, nummulites and orbitolinids.
test wall
465
FORAMINIFERA
Composed of low or high-Mg calcite, rarely of aragonite. - Very diverse in shape but common forms are circular to subcircular w/ chambers.
466
(Jurassic-Recent.) are planktonic algae w/c have lowMg calcite skeleton consisting of a spherical coccosphere (10-100µm diameter) composed of numerous calcareous plates, called coccoliths. - Coccoliths are chiefly disc-shaped, commonly w/ a radial arrangement of crystals. significant component of modern deep-water carbonate oozes, particularly those of lower latitudes, esp. in Tertiary and Cretaceous
Coccolithophorids
467
other term for Coccolithophorids
Chrysophyta
468
generally < 4 µm ✓ Lime mud is common in both modern and ancient ✓ Consists of microcrystalline calcite or aragonite ✓ In the modern, lime mud is derived from disaggregation of calcareous green algae which releases aragonite needles 1-5µm long ✓ Other possible sources or origin of micrite a. Inorganic precipitation b. Bioerosion where organisms such as boring sponges and microbes attack carbonate grains and substrates . Mechanical breakdown of skeletal grains thru waves and currents.
. Micrite
469
large crystals of Lo-Mg calcite that from cement in limestones
Sparry calcite
470
photic zone
(generally 0-30 m) is the most productive site for carbonate sediments, the socalled carbonate factor
471
year of folks
1959 1962
472
limestone formed in situ such as a stromatolite or reef-rock;
biolithite-
473
micrite w/ cavities such as birds-eye limestone
dismicrite
474
general term for fine-grained siliceous sediments of chemical, biochemical or biogenic origin.
Chert
475
for chert nodules occurring in Cretaceous chalks
Flint
476
fine-grained siliceous rocks w/ a texture and fracture similar to unglazed porcelain; also used for an opaline claystone composed largely of opal-C
Porcellanite
477
Three major groups of organisms that build their skeletons of silica:
Sponges-very important contributors of siliceous spicules to the sea-floor since the Paleozoic Radiolarians- marine planktonic protozoans; Paleozoic to Recent - skeleton or "tests" of opaline silica - live in near surface waters and feed of phytoplankton dominant sediment in the Equatorial Pacific beneath the CCD Diatoms- marine and non-marine; photosynthesing algae - live in the surface water - photosynthetic zone - since the early Cretaceous - principal component of marine phytoplanktons; a.k.a. "grass of the sea"; base of the food chain
478
also referred to as drusy quartz as it commonly occurs as a pore- filling cement
megaquartz
479
usually occur in a radiating arrangement * forming wedge-shaped, mammillated and spherulitic growth structures fibrous variety w/ crystals varying from a few tens to hundreds of microns in length
chalcedonic quartz
480
defined as sediments with > 15-20% P2O5; a source of fertilizer
Phosphatic Sediments
481
associated with regions of relatively high surface water fertility; accumulate near the edges of the oxygen minimum depth zone and is commonly a place where organic rich sediments like diatom ooze is being deposited
Phosphorites
482
deposits of organic material (mainly from phytoplanktons) in marine basins and lakes
Sapropels
483
forms during the accumulation of plant remains in anaerobic, watersaturated environment, generally in fresh water swamps and bogs in cool climates
peat
484
vascular (land) plant derived organic compounds altered by elevated temperature and burial pressure
Humic coal
485
Formed from non-vascular (algal) plant material
Sapropelic coal
486
sylvinite: mixture of sylvite, carnallite and halite -- fertilizer
potash
487
metastable; not preserved in rocks older than miTertiary; readily devitrified and replaced during weathering and diagenesis
Volcanic glass
488
smectite rich clay beds derived from the alteration of volcanic ash
Bentonite
489
hydrous sodium calcium aluminum silicates; formed from alteration volcanic glass, usually cryptocrystalline; often develop when ash has fallen into alkaline lakes
Zeolites
490
generally refers to beds thicker than 10 mm
beds: ✓ very thick bed > 1 m thick ✓ thick bed 1-0.3 m ✓ medium bed 0.3-0.1 m ✓ thin bed 0.1-0.01 m (overlap with thick lamina) ✓ very thin bed < 10 mm (overlap with medium lamina)
491
generally refers to beds thinner than 10 mm
laminae ✓ thick lamina 10-30 mm ✓ medium lamina 3-10 mm ✓ thin (fine) lamina 1-3 mm (e.g. Devonian Ratner of Sask) very thin (fine) lamina < 1 mm (deep sea and deep lake deposits, glacial lake varves)
492
(= ichnofossils = lebensspuren): traces of organism (commonly animal) activities and behavior (dwelling, feeding, locomotion, resting), not actual body fossils.
Trace fossils
493
MINERAL RESOURCES FROM SEDIMENTS
Banded iron formation (BIF) * Evaporite deposits (halite, gypsum, potassium and magnesium) * Placer deposits (gold, diamond, tin oxides) * Bauxite (aluminum; residual of clay deposits in tropical and subtropical regions) * Laterite (iron; residual soil; tropical weathering) * Magnetite * Fossil fuels (oil, natural gas, coal)
494
groundmass is made up rectangular formed feldspar instead of lath slender lath crystals
orthopyric
495
phenocrysts in a porphyritic texture are clustered into aggregates called glomerocrysts or crystals clots which indicates crystal fractionation by crystal settling
glomeroporphyritic
496
phenocrysts contain small grains of other minerals enclosing them indicating that the smaller grains may have crystallized first
poikilitic
497
variety of poikilitic texture where plag laths are enclosed by pyroxenes or olivine
ophitic
498
variety of ophitic wherein plag encloses ferromagnesian minerals indicating slower cooling in basaltic rocks
subophitic
499
also called corona reaction rim and rapakivi displays a secondary mineral formed around another mineral indicating a post magmatic reaction
opacitic
500
variety of opacitic where there is a secondary rim or corona
kelyphitic
501
occurs where crystal occupies occupy spaces between at least two larger crystals indicating a later formation
intergranular
502
denotes that angular spaces between crystals are filled with glass that may be devitrified or altered and small crystals
intersertal
503
holocrystalline groundmass with lath shaped microlites typically pla are generally oriented irregularly
pilotaxitic
504
extrusive igneous rock texture wherein the groundmass flow in the direction of lava flow and around inclusions and occurs in alkali rich rocks
trachytic
505
microscopic variety of trachytic that is visible to the naked eye
trachytoid
506
also called symplectic is an intergrowth of branching rods of quartz set in a single crystal of plag
myrmekitic
507
intergrowth of plag feldspar in alkali feldspar host
perthitic
508
intergrowth of alkali feldspar in plag feldspar host
holocrystalline
509
mix of glass and crystals but contains more crystals than glass
hypohyaline
510
contains 100% glass
holohyaline
511
contains very coarse grains having >30mm in diameter
pegmatitic
512
displays grains that are generally equant
granular
513
medium to coarse grained minerals most of which are devoid of crystal faces
granitic
514
contains equidimensional cryptocrystalline groundmass
felsitic
515
variety of poikilitic where in inclusions have a complete series of crystal sizes
seriate
516
loss or decrease in pressure which becomes the driving force of volcanoees to erupt causing the less dense magma material to rise and migrate to areas with less pressure
decompression
517
lowering of the melting temperature of the mantle due to the presence of fluxes causing earlier melting and production of the magma
flux melting
518
who devised the way of measuring the relative size or magnitude of volcanic eruptions ?
The Volcano Explositivity Index Newhall, C. and Self S. in 1982
519
steam eruptions that occur when water is heated by the country rock without having the need to be in contact with a magmatic body and erupts as a mixture of hot water and steam
phreatic
520
also called surseyan eruption is an explosive eruption produced when a magmatic body comes in contact with water causing rapid quenching and expansion of materials violently bursting into steam and volumes of ash
phreatomagmatic
521
effusive eruptions that produce large volumes of very hot thin runny lava that extrudes from fissures
icelandic
522
effusive eruptions similar to icelandic eruptions that originates from vents of volcanoes
hawaiian
523
explosive euptions that shoot thicker lava along with a burst of steam gas and ash that spatters molten lava
strombolian
524
series of discrete loud eruptions in throat clearing canon like explosions that shoor high velocity blocks and bombs
vulcanian
525
also called nuee ardente eruptions occur when large amount of tephra gas and lava are erupted laterally from the crated producing glowing avalanches
pelean
526
colossal explosive eruptions that involves very viscous magma and produce very large volumes of ash and tephra that can cover a very wide area
plinian
527
composed mostly of loose ejected ash and some lava appearing relatively symmetrical and steeply built with large deep craters with most being produced by a single eruptive event
pyroclastic cone
528
pyroclastic cones composed predominantly of vesicular basaltic material
scoria cone
529
pyroclastic cones with various compositions
cinder cone
530
volcanoes with an eruptive history that reached VE 8 or stronger
Supervolcano (yellowstone caldera)
531
give examples of extinct volcano, dormant volcano, inactive volcano and potentially active volcano
mt. chimborazo, ecuador mt. kilimanjaro tanzania alligator lake tadlac lake laguna mt. san cristobal laguna
532
short detached vesicle free proximal lava that are often produced by viscous lava such as andesitic and rhyolitic lava
block lava
533
a fractured surface texture formed when bombs cool
breadcrust texture
534
black glassy streamlined particles that formed as lava droplets that quenched in flight
pele's tears
535
golden acicular glassy strands that formed as lava droplets were propelled through the air being partially stretched into shape
pele's hair
536
usually associated with phreatic and pheratomagmatic eruptions and identified to have a pinch and swelling beds with moderate sorting of moderately rounded clasts
pyroclastic surge
537
generally hot flows made up of a mixture of pyroclastic materials and hot gases that can travel at rapid speeds
pyroclastic density currents
538
also known as cognate clasts are derived directly from magma involved in the volcanic activity
juvenile clasts
539
rock inclusions from the vent wall or brought from the surface by lava or pyroclastic walls
accidental clasts
540
fragmentation through explosive ejection and aerial dispersal of pyroclasts of rock and magma from a volcanic vent
autoclastic process
541
fragmentation brought by the weathering and disintegration of volcanic rocks
epiclastic process
542
clasts within the mass flow behaving independently in moving interstitital fluids
traction transport
543
a hot mixture of volcanic debris and tephra that is saturated with water that occurs directly related to an on going eruption
syn eruption lahar
544
also known as large igneous provinces or LIPS are products of massive outpourings of low viscosity basaltic lava that envelop hundreds of thousands of square kilometers
flood basalt
545
airborne blobs of liquid lava emitted by lava fountaining
spatter
546
also called welded spatter are spatters that solidified at the base of the lava fountain
agglutinate deposits
547
cones produced when welded spatters accumulate around a central vent that can typically grow less than 20m in height
spatter cone
548
linear ridges formed when lave fountains erupt via fissures
spatter ramparts
549
smaller tuff rings
tuff cone
550
glassy volcanic debris and scoria develop die to the explosive eruption of basalt in a water
tuff ring
551
when was PHIVOLCS established
September 17, 1984