What is a volcano?
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What is a volcano?. A hill with a crater? Does magma need to be involved? Does it matter?.

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What is a volcano

What is a volcano?

A hill with a crater?

Does magma need to be involved?

Does it matter?

Lecture material about Introduction to Volcanology, covering, Heat in the earth, where magma comes from and how, earth’s mantle, tectonics and convection, basalt and why it is fundamental, where volcanoes are.

Thanks to Wendy Bohrson and Glen Mattioli who provided many of the slides.


Magma plumbing system

Magma Plumbing System

  • Melts form in mantle

  • Pool in magma chambers

  • Magma eventually erupts


What is a volcano

Volcanology

Study of generation of magma, transport of magma, and shallow-level or surface processes that result from intrusion and eruption of magma


What is a volcano

Volcanology

  • Physical and chemical behavior of magmas

  • Transport and eruption of magma

  • Formation of volcanic deposits


What is a volcano

What do we need for volcanism?

  • Thermal energy

  • Material to melt

  • Ability to erupt


Earth s energy budget

Earth’s Energy Budget

  • Solar radiation: 50,000 times greater than all other energy sources; primarily affects the atmosphere and oceans, but can cause changes in the solid earth through momentum transfer from the outer fluid envelope to the interior

  • Radioactive decay:238U, 235U, 232Th, 40K, and 87Rb all have t1/2 that >109 years and thus continue to produce significant heat in the interior; this may equal 50 to 100% of the total heat production for the Earth. Extinct short-lived radioactive elements such as 26Al were important during the very early Earth.

  • Tidal Heating: Earth-Sun-Moon interaction; much smaller than radioactive decay

  • Primordial Heat: Also known as accretionary heat; conversion of kinetic energy of accumulating planetismals to heat.

  • Core Formation: Initial heating from short-lived radioisotopes and accretionary heat caused widespread interior melting (Magma Ocean) and additional heat was released when Fe sank toward the center and formed the core


What is a volcano

What are the sources of heat within Earth?

  • Primordial/accretional energy

  • Radioactive decay


Natural radioactivity

“Natural” Radioactivity

  • Elements (determined by Z) typically exist as a mix of isotopes which have different atomic weights (eg 39K and 40K, where Z=19).

  • Isotopes may be stable, radioactive or radiogenic.

  • 39K is stable, 40K is radioactive, 40A and 40Ca radiogenic.

  • Decay of radioactive isotopes has a very predictable rate: N = Noe-t .

  • This decay occurs spontaneously everywhere and is not influenced by changes in T, P or composition!

  • Decay reactions of many types occur: 40K-> 40Ca + electron + heat.

  • Discovered by Marie Curie.


What is a volcano

Natural Radioactivity is exploited by volcanologists and petrologists.

Radiometric dating. System of 40K->40A leads to K/A and A/A dating methodology. These use the age eqn and depend on purging of A at time of eruption.

Radioactive Tracing. Use isotopic ratios of elements to tell where the magma came from. Ex: 87Sr/86Sr this is radiogenic/stable, so it can measure the amounts of radioactive parent= 87Rb


Rates of heat production and half lives

Rates of Heat Production and Half-lives


What is a volcano

dN

dN

-

µ

-

l

N or

=

N

dt

dt

Radioactive Decay

The Law of Radioactive Decay

# parent atoms

time 


What is a volcano

D = Nelt - N= N(elt -1)

age of a sample (t) if we know:

D the amount of the daughter nuclide produced

N the amount of the original parent nuclide remaining

l the decay constant for the system in question


What is a volcano

The K-Ar System

40K  either 40Ca or 40Ar

  • 40Ca is common. Cannot distinguish radiogenic

    40Ca from non-radiogenic 40Ca

  • 40Ar is an inert gas which can be trapped in

    many solid phases as it forms in them


What is a volcano

l

æ

ö

e

ç

÷

è

ø

l

The appropriate decay equation is:

40Ar = 40Aro + 40K(e-lt -1)

Where le = 0.581 x 10-10 a-1 (electron capture)

and l = 5.543 x 10-10 a-1 (whole process)


What is a volcano

  • Blocking temperatures for various minerals differ

  • 40Ar-39Ar technique grew from this discovery


Heat production through earth history

Heat Production through Earth History


Earth structure

Earth Structure


What is a volcano

How do we know the composition of the mantle?

  • Peridotite bodies (e.g., ophiolites)

  • Xenoliths

  • Cosmochemical Evidence/Meteorites


What is a volcano

Ophiolites

Seismic velocity is plotted on the horizontal axis versus depth below the seafloor on the vertical axis. The different seismic layers are marked on the plot with geologic interpretations of the rock units. The layers are defined by velocities and velocity gradients. Cross section through a typical ophiolite sequence is shown to the right.

http://www.womenoceanographers.org/doc/KGillis/Lesson/gillis_lesson.htm


What is a volcano

Ophiolites

Picture of a hillside in Cyprus. The vertical slabs of rock are dikes intruding into lavas that erupted on the seafloor. This section represents the transition from lavas to sheeted dikes and is thought to correspond to seismic Layer 2B as seen in Figure 5. Taken from the RIDGE field school in Cyprus.

http://www.womenoceanographers.org/doc/KGillis/Lesson/gillis_lesson.htm


What is a volcano

Mantle Xenoliths

http://www.nhm.ac.uk/mineralogy/petrology/MantleXenoliths.htm


What is a volcano

Carbonaceous Chondrites

Left to right: fragments of the Allende, Yukon, and Murchison meteorites

http://www.daviddarling.info/encyclopedia/C/carbchon.html


What is a volcano

Mantle vs Model CC


What is a volcano

Composition of the Mantle

What is the mineralogy of the mantle?

Olivine +clinopyroxene + orthopyroxene ± plagioclase, garnet, spinel (Al bearing minerals)


What is a volcano

Mineralogy of Mantle


What is a volcano

crust

obvious from space that Earth has two fundamentally different

physiographic features: oceans (71%) and continents (29%)

from: http://www.personal.umich.edu/~vdpluijm/gs205.html

global topography


Differentiation of the earth

Differentiation of the Earth

  • Melts extracted from the mantle rise to the crust, carrying with them their “enrichment” in incompatible elements

    • Continental crust becomes “incompatible element enriched”

    • Mantle becomes “incompatible element depleted”

From: http://www.geo.cornell.edu/geology/classes/geo302


Radioactivity in earth materials

Radioactivity in earth materials

Heat production decreases with depth from crust to mantle.


Earth s geothermal gradient

Earth’s Geothermal Gradient

Average Heat Flux is

0.09 watt/meter2

Geothermal gradient = DT/ Dz

20-30°C/km in orogenic belts;

Cannot remain constant w/depth

At 200 km would be 4000°C

~7°C/km in trenches

Viscosity, which measures

resistance to flow, of mantle

rocks is 1018 times tar at 24°C !

Approximate Pressure (GPa=10 kbar)


Earth interior pressures

Earth Interior Pressures

  • P = rVg/A = rgz, if we integrate from the surface to some

  • depth z and take positive downward we get

  • DP/Dz = rg

Rock densities range from 2.7 (crust) to 3.3 g/cm3 (mantle)

270 bar/km for the crust and 330 bar/km for the mantle

At the base of the crust, say at 30 km depth, the lithostatic pressure

would be 8100 bars = 8.1 kbar = 0.81 GPa


Gravity pressure and the geobaric gradient

Gravity, Pressure, and the Geobaric Gradient

  • Geobaric gradient defined similarly to geothermal gradient: DP/Dz; in the interior this is related to the overburden of the overlying rocks and is referred to as lithostatic pressure gradient.

  • SI unit of pressure is the pascal, Pa and 1 bar (~1 atmosphere) = 105 Pa

  • Pressure = Force / Area and Force = mass * acceleration

  • P = F/A = (m*g)/A and r (density) =mass/volume


Heat flow on earth

Heat Flow on Earth

An increment of heat, Dq, transferred into a body produces a

Proportional incremental rise in temperature, DT, given by

Dq = Cp * DT

where Cp is called the molar heat capacity of J/mol-degree

at constant pressure; similar to specific heat, which is based

on mass (J/g-degree).

1 calorie = 4.184 J and is equivalent to the energy necessary

to raise 1 gram of of water 1 degree centigrade. Specific heat

of water is 1 cal/g°C, where rocks are ~0.3 cal/g°C.


Heat transfer mechanisms

Heat Transfer Mechanisms

  • Radiation: involves emission of EM energy from the surface of hot body into the transparent cooler surroundings. Not important in cool rocks, but increasingly important at T’s >1200°C

  • Advection: involves flow of a liquid through openings in a rock whose T is different from the fluid (mass flux). Important near Earth’s surface due to fractured nature of crust.

  • Conduction: transfer of kinetic energy by atomic vibration. Cannot occur in a vacuum. For a given volume, heat is conducted away faster if the enclosing surface area is larger.

  • Convection: movement of material having contrasting T’s from one place to another. T differences give rise to density differences. In a gravitational field, higher density (generally colder) materials sink.


Magmatic examples of heat transfer

Magmatic Examples of Heat Transfer

Thermal Gradient =DT between

adjacent hotter and cooler masses

Heat Flux = rate at which heat is

conducted over time from a unit

surface area

Thermal Conductivity = K; rocks

have very low values and thus

deep heat has been retained!

Heat Flux = Thermal Conductivity * DT


What is a volcano

Types of Thermal Energy Transfer

Models of Earth’s interior converge on core Ts of 4000°C ± 500 °C

Thermal energy moves from hot to cold--> thus, modes of energy transport within Earth:

  • Conduction

  • Convection

  • Radiation


Earth structure1

Earth Structure


What is a volcano

How do we know that convection is important?

Thought experiment:

Distance heat transported by conduction =

sqrt (thermal diffusivity * age of Earth)

  • Thermal diffusivity = 10-6 m2/s

  • 3.2 x 107 sec/yr


What is a volcano

How do we know that convection is important?

10-6 m2/s * 4.5 x 109 yr * 3.2 x 107 sec/yr =

380 km

Radius of Earth = 6371 km

Conclusion: barely any heat transported by conduction. Requires a convective mechanism.


Convection examples

Convection Examples


Rayleigh bernard convection

Rayleigh-Bernard Convection


Convection in the mantle

Convection in the Mantle


What is a volcano

models

from: http://www.geo.lsa.umich.edu/~crlb/COURSES/270

convection in the mantle

observed heat flow

warmer: near ridges

colder: over cratons

from: http://www-personal.umich.edu/~vdpluijm/gs205.html


What is a volcano

examples from western Pacific

blue is high velocity (fast)

…interpreted as slab

note continuity of blue slab

to depths on order of 670 km

from: http://www.pmel.noaa.gov/vents/coax/coax.html


Earth s plates

Earth’s Plates


Where volcanoes occur

Where Volcanoes Occur


What is a volcano

Volcano geography

1. Divergent margins 2. Convergent margins

3. Intraplate 4. Hotspots


What is a volcano

Plate tectonics and magma composition

1. Divergent margins: Plate separation and decompression melting -> low volatile abundance, low SiO2 (~50%), low viscosity basaltic magmas (e.g. Krafla, Iceland)

2. Convergent margins : Mixtures of basalt from the mantle, remelted continental crust and material from the subducted slab. High volatile abundance, intermediate

SiO2 (60-70%), high viscosity andesites and dacites (e.g. Montserrat, West Indies)

3. Intraplate `Hot-spot` settings:

A. Oceanic: Mantle plumes melt thin oceanic crust producing low viscosity basaltic magmas (e.g. Kilauea, Hawaii)

B. Continental: Mantle plumes melt thicker, silicic continental crust producing highly silicic (>70% SiO2) rhyolites (e.g. Yellowstone, USA)


What are the plate tectonic settings in which magmatism occurs

What are the plate tectonic settings in which magmatism occurs?


What is a volcano

Processes of Partial Melting

Precursor to all igneous rocks is magma or melt (liquid rock)

How does melting occur?


What is a volcano

Processes of Partial Melting

Let’s first look at a phase diagram (P-T) diagram of mantle


What is a volcano

Processes of Partial Melting

A simpler phase diagram (P-T) diagram of mantle


What is a volcano

Processes of Partial Melting

What causes partial melting in the mantle?

Two processes:

  • Lowering of solidus by volatile addition

  • Adiabatic Decompression


What is a volcano

Processes of Partial Melting

Lowering solidus by volatile addition

Temperature


What is a volcano

Processes of Partial Melting

Adiabatic Decompression

Pressure


What is a volcano

The Mantle

Why is melting in the mantle important?

Because most of the melts that make extrusive rocks on Earth originate in the mantle


Earth s geothermal gradient1

Earth’s Geothermal Gradient

Average Heat Flux is

0.09 watt/meter2

Geothermal gradient = DT/ Dz

20-30°C/km in orogenic belts;

Cannot remain constant w/depth

At 200 km would be 4000°C

~7°C/km in trenches

Viscosity, which measures

resistance to flow, of mantle

rocks is 1018 times tar at 24°C !

Approximate Pressure (GPa=10 kbar)


Mechanisms of melt formation

Mechanisms of melt formation

  • MOR = Adiabatic decompressionIntraplate = adiabatic decompressionConvergent = change in solidus by volatile fluxing


Divergent settings the mid ocean ridge

Divergent settings: The Mid-ocean Ridge


Bathymetry of the east pacific rise

Bathymetry of the East Pacific Rise


Magma chamber structure beneath east pacific rise

Magma Chamber Structure beneath East Pacific Rise

Volcanic layer transitions into sheeted dike zone, which represents feeder zone from magma chamber.

Below is a sill-like magma body (1-2 km depth) that transitions to crystal mush (partially solidified zone >50% crystals).

Transitional zone is solidified but hot gabbro.


Morb genesis

MORB Genesis


Intraplate settings mantle plumes

Intraplate settings: Mantle Plumes


Proposed hot spot traces

Proposed Hot Spot Traces


Magma plumbing system for hawaii

Magma Plumbing System for Hawaii

Zone of partial melting at depth (>100 km)

Magma ascends through conduit system

Presence of summit reservoir and rift zones


Shallow magma plumbing system

Shallow Magma Plumbing System


Geometry of magma reservoir beneath kilauea

Geometry of Magma Reservoir beneath Kilauea


Convergent settings subduction zone magmatism

Convergent settings: Subduction Zone Magmatism


Characteristics of subduction zone magmatism

Characteristics of Subduction Zone Magmatism

Down-going, hydrated slab undergoes metamorphism and dehydration

Fluids infiltrate overlying mantle “wedge”

Reduces solidus and melting can occur

Produces arc magmatism


Relative volumes

Relative Volumes


What are the relative volumes of eruption and intrusion

What are the relative volumes of eruption and intrusion?


What are the relative volumes of eruption and intrusion1

What are the relative volumes of eruption and intrusion?


Volumes of igneous rocks on earth

Volumes of Igneous Rocks on Earth


Convergent margin magma genesis

Convergent Margin Magma Genesis


Classification of igneous rocks

Classification of Igneous Rocks

Figure 2-4. A chemical classification of volcanics based on total alkalis vs. silica. After Le Bas et al. (1986) J. Petrol., 27, 745-750. Oxford University Press.


Basalt types major element variation

Basalt Types-Major Element Variation


Alkaline and subalkaline rock suites

Alkaline and Subalkaline Rock Suites

15,164 samples

Irregular solid line defines the boundary between Ne-norm rocks

Le Bas et al., 1992; Le Roex et al., 1990; Cole, 1982; Hildreth & Moorbath, 1988


K 2 o content of subalkaline rocks

K2O content of subalkaline rocks

K2O content

may broadly

correlate with

crustal thickness.

Low-K 12 km

Med-K 35 km

High-K 45 km

Ewart, 1982


Yoder tilley basalt tetrahedron

Yoder & Tilley Basalt Tetrahedron

Yoder & Tilley, 1962; Le Maitre


Terrestrial basalt generation summary

Terrestrial Basalt Generation Summary

  • MORBs are derived from the partial melting of a previously depleted upper mantle under largely anhydrous conditions at relatively shallow depths.

  • True primary mantle melts are rare, although the most primitive alkali basalts are thought to represent the best samples of direct mantle melts.

  • The trace element and isotopic ratio differences among N-MORB (normal), E-MORB (enriched), IAB, and OIB indicate that the Earth’s upper mantle has long-lived and physically distinct source regions.

  • Ancient komatiites (>2.5 Ga) indicate that the Earth’s upper mantle was hotter in the Archean, but already depleted of continental crustal components.


Lunar surface

Lunar Surface


Apollo 15 basalt sample

Apollo 15 Basalt Sample

Vesicles -

Probably

derived from

CO degassing


Lunar olivine basalt thinsection

Lunar Olivine Basalt Thinsection

Fe-Ti oxides

Plagioclase

Olivine + aligned MIs

Pyroxenes

Plane Polarized Light

Sample collected from the SE end of

Mare Procellarum by the Apollo 12 mission.

Interpreted as a Lava Lake basalt.

Cross Polarized Light

From: http://www.union.edu/PUBLIC/GEODEPT/COURSES/petrology/moon_rocks/12005.htm


Lunar anorthosite thinsection

Lunar Anorthosite Thinsection

Pyroxenes

Fractured Plagioclase Feldspar

Rock is 98% fsp,

An95 to An97

Plane Polarized Light

Highly brecciated lunar anorthosite was

collected by the Apollo 16 mission to the

lunar highlands SW of Mare Tranquillitatis.

It has been dated at 4.44 Ga.

Cross Polarized Light

From: http://www.union.edu/PUBLIC/GEODEPT/COURSES/petrology/moon_rocks/12005.htm


Earth mars sized impact model for lunar origin

Earth Mars-sized Impact Model for Lunar Origin

Impact + 0.5 hr

Impact + 5hr

From: Kipp & Melosh, 1986 (above) and W. Hartmann paintings of Cameron, Benz, & Melosh models (right)


Features of the giant impact hypothesis

Features of the Giant Impact Hypothesis

  • Original idea paper by Hartmann & Davis, 1975; additional geochemical research by Michael Drake and computer models by Jay Melosh and colleagues.

  • Impact occurs soon after Earth’s core formation event because of the small lunar Fe core and difference in bulk density (rMoon = 3.3 g/cc << rEarth = 5.5 g/cc).

  • Impact event must occur before formation of the lunar highlands at 4.4 Ga, which formed as a result of the crystallization of the lunar magma ocean. Lunar differentiation continues w/ basalt genesis (3.95 to 3.15 Ga).

  • Oxygen isotope compositions of lunar and terrestrial rocks are similar, but different from Mars and meteorites. Earth-Moon must be made of the same stuff.

  • Volatiles are depleted in the proto-moon during impact event. This is consistent with geochemistry and petrology of lunar samples.


Lunar interior composition

Lunar Interior Composition

From: BVSP, 1986 and Taylor, 1987


1984 mauna loa eruption

1984 Mauna Loa Eruption


Curtain of lava

Phase 1: Pu’u O’o

Curtain of lava


Phase 1 pu u o o

Phase 1: Pu’u O’o

Fire Fountain


Pu u o o vent with pahoehoe flows

Pu’u O’o Vent with pahoehoe flows


Pahoehoe flow kilauea

Pahoehoe flow, Kilauea


Tree molds 1983

Tree Molds, ~1983


Halemaumau kilauea

Halemaumau, Kilauea


Surtsey iceland

Surtsey, Iceland

A new volcanic island formed in 1966


Cerro negro nicaragua

Cerro Negro, Nicaragua


Stromboli volcano italy

Stromboli Volcano, Italy


Paricutin mexico

Paricutin, Mexico

1943-1954


Mt augustine alaska

Mt. Augustine, Alaska


Augustine

Augustine

Note hummocky topography from debris avalanche, 1883


Eruption of mt augustine 1986

Eruption of Mt. Augustine, 1986


Crater lake

Crater Lake


Crater lake1

Crater Lake


Ol doinyo lengai

Ol Doinyo Lengai

A sodium carbonatite volcano in the Rift Valley of East Africa


Ol doinyo lengai1

Ol Doinyo Lengai

A sodium carbonatite volcano in the Rift Valley of East Africa


Olympus mons mars

Olympus Mons, Mars

A giant Martian volcano 25 km high and 700 km wide. The Island of Maui in Hawaii would fit inside the huge caldera of Olympus Mons.


Sources

Sources

  • http://www.doubledeckerpress.com/archive.htm

  • http://pubs.usgs.gov/gip/volc/types.html

  • http://hvo.wr.usgs.gov/

  • http://cvo.wr.usgs.gov/


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