Igneous Activity and Plate Tectonics Chapter Three Igneous Activity and Plate Tectonics

The Rock Cycle A rock is a naturally formed, consolidated material usually composed of grains of one or more minerals The rock cycle shows how one type of rocky material gets transformed into another Representation of how rocks are formed, broken down, and processed in the geosphere Arrows indicate possible process paths within the cycle

CHAPTER – 3 IGNEOUS ROCKS *IGNEOUS ROCKS: ROCKS THAT COOLED AND FIRE CRYSTALLIZED DIRECTLY FROM MOLTEN ROCK, EITHER AT THE SURFACE OR DEEP UNDERGROUND *MAGMA: MOLTEN ROCK WITHIN THE EARTH *LAVA: WHEN MAGMA REACHES EARTH’S SURFACE *MOST IGNEOUS PROCESSES ARE HIDDEN FROM VIEW *REGIONAL EROSION EXPOSES ANCIENT IGNEOUS EVENTS :

DISTRIBUTION OF MAJOR CONTINENTAL IGENOUS ROCKS

MOLTING ROCKS AND CRYSTALLIZING MAGMA MAGMA FORMATION: HEATED UNGERGROUND MINERALS – BONDS BROKEN- BECOMES MAGMA – CHEMICAL COMPOSITION OF MAGMA CHANGES MAGMA COOLING AND CRYSTALLIZATION: AS COOLING PROGRESSES, DIFFERENT MINERALS CRYSTALLIZE  

EFFECT ON THERMAL ENERGY

The Rock Cycle and Plate Tectonics Magma is created by melting of rock above a subduction zone Less dense magma rises and cools to form igneous rock Igneous rock exposed at surface gets weathered into sediment Sediments transported to low areas, buried and hardened into sedimentary rock Sedimentary rock heated and squeezed at depth to form metamorphic rock Metamorphic rock may heat up and melt to form magma Convergent plate boundary

CLASSIFICATION OF IGNEOUS ROCKS: TEXTURE: SIZE AND SHAPE OF MINERAL CRYSTALS CRYSTAL GROWTH DURING COOLING MINERAL CONTENT:CHEMICAL COMPOSITION COOLING HISTORY TEXTURE: RATE AT WHICH MAGMA OR LAVA COOL WHEN 100 – 1000 YRS FOR COOLING TIME TO GROW LARGER CRYSTALS  CRYSTALS CAN BE VISIBLY SEEN  PHANERTIC TEXTURE   INTRUSIVE ROCKS (OR PLUTONIC ROCKS) SLOW COOLING OCCURS WHEN MAGMAS INTRUDE PREEXISTING SOLID ROCKS

Igneous Rocks Magma is molten rock Igneous rocks form when magma cools and solidifies Intrusive igneous rocks form when magma solidifies underground Granite is a common example Extrusive igneous rocks form when magma solidifies at the Earth’s surface (lava) Basalt is a common example Granite Basalt

PEGMATITES: IGNEOUS ROCKS WITH EXCEPTIONALLY LARGE CRYSTALS (QUARTZ, MICA, FELDSPAR ARE COMMON) EXTRUSIVE OR VOLCANIC ROCKS: WHEN ROCKS SOLIDIFY QUICKLY, CRYSTALS ARE SMALL APHANITIC TEXTURE – ROCKS WITH AHANITIC STRUCTURE ARE CALLED EXTRUSIVE ROCKS PORPHYRITIC STRUCTURE: LARGER AND SMALLER GRAINS – SLOW COOLING FOLLOWED ABRUPTLY BY RAPID COOLING

VOLCANIC GLASS: WHEN LAVA SUDDENLY COOLS, NO TIME TO FORM CRYSTALS *VOLCANIC GLASS: WHEN LAVA SUDDENLY COOLS, NO TIME TO FORM CRYSTALS. TEXTURE IS GLASSY. *PUMICE: FORMS WHEN HIGHLY GASEOUS, SILICA – RICH LAVA COOLS VERY RAPIDLY *OBSIDIAN: VERY Si-RICH LAVAS CONTAINING LESS GAS, COOL VERY QUICKLY  

Igneous Rock Textures Texture refers to the size, shape and arrangement of grains or other constituents within a rock Texture of igneous rocks is primarily controlled by cooling rate Extrusive igneous rocks cool quickly at or near Earth’s surface and are typically fine-grained (most crystals <1 mm) Intrusive igneous rocks cool slowly deep beneath Earth’s surface and are typically coarse-grained (most crystals >1 mm) Coarse-grained igneous rock Fine-grained igneous rock

Special Igneous Textures A pegmatite is an extremely coarse-grained igneous rock (most crystals >5 cm) formed when magma cools very slowly at depth A glassy texture contains no crystals at all, and is formed by extremely rapid cooling A porphyritic texture includes two distinct crystal sizes, with the larger having formed first during slow cooling underground and the small forming during more rapid cooling at the Earth’s surface Pegmatitic igneous rock Porphyritic igneous rock

IGNEOUS COMPOSITION MAGMA  O2, Si, Al, Fe, Ca, Mg, Na, K, S. DISSOLVED GASSES  WATER VAPOR, CO2, SO2. SILICATES ARE THE MAJOR CONSTITUENTS OF IGNEOUS ROCKS

Igneous Rock Identification Igneous rock names are based on texture (grain size) and mineralogic composition Textural classification Plutonic rocks (gabbro-diorite-granite) are coarse-grained and cooled slowly at depth Volcanic rocks (basalt-andesite-rhyolite) are typically fine-grained and cooled rapidly at the Earth’s surface Compositional classification Mafic rocks (gabbro-basalt) contain abundant dark-colored ferromagnesian minerals Intermediate rocks (diorite-andesite) contain roughly equal amounts of dark- and light-colored minerals Felsic rocks (granite-rhyolite) contain abundant light-colored minerals

CLASSIFICATION OF IGNEOUS ROCKS AND MAGMAS COMPOSITION   TYPE Si ( % ) OTHER MAJOR ELEMENTS VISC. OF MAGMA IGNEOUS ROCKS PRODUCED FELSIC >65 Al, K, Na HIGH ~ 600 – 800 0C INTERMEDIATE 55-65 Al, Ca, Na, Fe, Mg MEDIUM ~ 800 – 1000 0C MAFIC (BASALT) 45 - 55 Al, Ca, Fe, Mg LOW ~ 1000 – 1200 0C ULTRAMARIC (PERIDOTITE) < 40 VERY LOW > 1200 0C

IGNEOUS ROCK - CHART

ULTRA MAFIC IGNEOUS ROCKS: * < 40% Si. * EX: PERIDOTITE & KOMATITE * OCCURRENCE: RARE AT EARTH’S SURFACE MAFIC IGNEOUS ROCKS: * 45 – 55 % Si. * EX: BASALT & GABBRO * OCCURRENCE: COMMON ON OCEAN FLOORS AND CONTINENTS INTERMEDIATE IGNEOUS ROCKS: * 55 – 65 % Si. *EX: ANDESITE & DIORITE * OCCURRENCE: ABUNDANT VOLCANIC ROCK.   FELSIC IGNEOUS ROCKS: * > 65% Si. * EX: GRANITE & RHYOLITE * OCCURRENCE: COMMON ON CONTINENTS

CREATION OF MAGMA: THERMAL ENERGY * PARTIAL MELTING    WHEN ROCKS MELT TO PRODUCE MAGMA  PARTIAL MELTING  DIFF. MELTING POINT EX: ALBITE = 1118 0C ANORTHITE = 1553 0C * MELTING OF ROCKS DEPENDS ON  HEAT  PRESSURE  AMOUNT OF H2O IN THE ROCKS. THERMAL ENERGY

HEAT SOURCES *HEAT: SOURCE OF HEAT IN THE INTERIOR   * DECAY OF RADIOACTIVE ISOTOPES *RESIDUAL FROM EARTH’S FORMATION *FRICTIONAL HEAT FROM PLATE MOTION   *HIGH PRESSURE: THE IONS AND ATOMS IN A CRYSTALLINE SOLID CLOSER TOGETHER – HIGH TEMP IS REQUIRED TO VIBRATE, WEAKEN, AND BREAK THEIR BONDS. *AS PRESSURE INCREASES, THE TEMPERATURE AT WHICH ROCKS MELT INCREASES EX: Na – FELDSPAR ALBITE MELTS AT 1118 0C AT 100 KM PRESSURE IS 35, 000 TIMES HIGHER–MP 1440 0C

GEOTHERMAL GRADIENT

MELTING TEMPERT.-DRY

MELTING TEMPERT.-WET

FLUIDITY AND VISCOSITY OF MAGMA: MAGMA RISES BECAUSE    IF IT IS LESS DENSE THAN SURROUNDING ROCK  EXPANDING GASES DRIVE IT UPWARD  IT IS SQUEEZED UPWARD BY SURROUNDING ROCKS VISCOSITY: FLUID RESISTANCE TO FLOW      A) INCREASES WITH DECREASING TEMPERATURE       B) MINERAL (SILICA) CONTENT INCREASES VISCOSITY VALUE.

CRYSTALLIZATION OF MAGMA: *MINERALS MELT AT THE SAME TEMPERATURE AT WHICH THEY CRYSTALLIZE  FIRST TO MELT  LAST TO CRYSTALLIZE * AT EACH STAGE OF COOLING,   CRYSTAL/LIQUID RATIO CHANGES  

OCEANIC PLATE SUBDUCTS

MAGMA MIXING

BOWEN’S REACTION SERIES: A)     BOTH MAFIC AND FELSIC ROCKS CAN CRYSTALLIZE FROM AN ORIGINALLY MAFIC MAGMA B)      EARLY – FORMING CRYSTALS REMAINING IN CONTACT WITH THE STILL – LIQUID MAGMA REACT WITH IT TO EVOLVE INTO DIFFERENT MINERALS

BOWEN’S REACTION SERIES

Bowen’s Reaction Series Minerals crystallize in a predictable order, over a large temperature range Discontinuous branch Ferromagnesian minerals (olivine, pyroxene, amphibole, biotite) crystallize in sequence with decreasing temperature As one mineral becomes chemically unstable in the remaining magma, another begins to form Continuous branch Plagioclase feldspar forms with a chemical composition that evolves (from Ca-rich to Na-rich) with decreasing temperature

EARLY-FORMING CRYSTALS

MAGMA & EARLY FORMING CRYSTALS

SILICATE MINERALS CAN CRYSTALLIZE FROM MAFIC MAGMAS TWO WAYS: DISCONTINUOUS SERIES   OLIVINE PYROXINE AMPHIBOLE BIOTITE MICA MINERALS WITHOUT Fe, Mg. CONTINUOUS SERIES CALCIUM PLAGIOCLASE SODIUM PLAGIOCLASE

CONTD- *AFTER BOTH SERIES COMPLETE, HIGH – SILICA MINERALS FORM EX: K – FELDSPAR MUSCOVITE MICA QUARTZ  

HOW MAGMA CHANGES AS IT COOLS: CRYSTALS CAN * REMAIN SUSPENDED AND REACT WITH MAGMA * SINK * BE PLASTERED TO THE WALLS OR CEILING OF THE MAGMA *BE FILTERED OUT AS MAGMA FLOWS ELSEWHERE OTHER MAGMA CRYSTALLIZATION PROCESSES: * OTHERS – ASSIMILATION OF ROCK BODIES * MAGMA MIXING 1.

INTRUSIVE ROCK FORMATION: RISING MAGMA MAY FORCE OVERLYING ROCKS TO BULGE UPWARD  RESULTING ROCK APPEARS AS A DOOMED INTRUSION WITHIN OTHER ROCKS  THIS STRUCTURE IS KNOWN AS DIAPIR   XENOLITHS: WHEN PREEXISTING ROCK IS ASSIMILATED IN A MAGMA, THEY APPEAR IN THE SOLIDIFIED ROCK AS DISTINCT BODIES – XENOLITHS

PLUTONS: MAGMA THAT COOL UNDERGROUND FORM PLUTONS CONCORDANT PLUTONS: DISCORDANT PLUTONS: TABULAR PLUTONS PARALLEL TO THE PREEXISTING ROCK LAYERS – CALLED “SILLS” CUT ACROSS THE PREEXISTING LAYERS – CALLED “DIKES” MASSIVE SIZE BATHOLITHS RELATIVELY THIN

TABULAR PLUTONS DIKES SILLS – DISTINGUISHED FROM EXTRUSIVE FLOWS BY   A)EVIDENCE OF HEATING OF ADJACENT ROCK SURFACES B)EVIDENCE OF INCLUSIONS OF COUNTRY ROCK IN BOTH UPPER & LOWER SILL SURFACE C)LACK OF VESICLES ( HOLES FROM GAS BUBBLES ) ON UPPER SURFACE D)LACK OF WEATHERING OF LARGE SURFACE.

PLUTONIC IGNEOUS FEATURES

BATHOLITHS AND LARGE PLUTONS: 1.        LACCOLITHS 2.        LAPOLITHS     3.        BATHOLITHS A)DEFINITION B)EXAMPLES C)TEXTURE

SEMINARY RIDGE TOPOGRAPHIC RIDGE

SILLS AND LAVA FLOWS

LACCOLITH

PLATE TECTONICS AND IGNEOUS ROCKS: A) THE ORIGIN OF BASALT & GABBROS   1) INTRODUCTION * UPPER MANTLE LACKS LIGHT ELEMENTS *DEEPER MANTLE POSSESSES SOME LIGHT ELEMENTS *PRESENCE OR ABSENCE OF LIGHT ELEMENTS IN GABBRO & BASALT IDENTIFIES SOURCE OF PARENT MAGMA

Igneous Activity and Plate Tectonics Igneous activity occurs primarily at or near tectonic plate boundaries Mafic igneous rocks are commonly formed at divergent boundaries Increased heat flow and decreased overburden pressure produce mafic magmas from partial melting of the asthenosphere Intermediate igneous rocks are commonly formed at convergent boundaries Partial melting of basaltic oceanic crust produces intermediate magmas

Igneous Activity and Plate Tectonics Felsic igneous rocks are commonly formed adjacent to convergent boundaries Hot rising magma causes partial melting of the granitic continental crust Intraplate volcanism Rising mantle plumes can produce localized hotspots and volcanoes when they produce magmas that rise through oceanic or continental crust Hawaii is an example

PLATE SETTINGS & BASALTS

BASALTS-OCEAN & LAND 2) OCEANIC BASALTS 3) CONTINENTAL BASALTS   a) MORBS FROM UPPER MANTLE b)OIBS ( OCEAN ISLAND BASALTS) FROM DEEPER MANTLE 3) CONTINENTAL BASALTS a) COMPOSITION VARIES WIDELY b) BASALTS NEAR CONTINENTAL RIFTS FROM DEEP MANTLE c)BASALTS NEAR SUBDUCTION ZONES FROM UPPER MANTLE

ANDESITE & DIORITE ORIGIN

B) ORIGIN OF ANDESITES & DIORITE PROXIMITY TO SUBDUCTION ZONES FACTORS IN FORMATION   a) WATER CONTENT b) ASSIMILATION OF COUNTRY ROCKS c) OCEANIC SEDIMENTS C) ORIGIN OF RHYOLITES & GRANITES NEARLY ALL FOUND ON CONTINENTS DERIVE FROM PARTIAL MELTING OF LOWER CONTINENTAL CRUST EXIST NEAR MODERN OR ANCIENT SUBDUCTION ZONES

GEOLOGY AT A GLANCE

CHAPTER SUMMARY MAGMA, LAVA, DIFFERENCE BETWEEN THEM   MAGMA, LAVA, DIFFERENCE BETWEEN THEM PROPERTIES TO IDENTIFY IGNEOUS ROCKS FACTOR(S) THAT GOVERN ROCK TEXTURE APHANITIC, PHANERTIC, PLUTONIC, PORPHYRITIC MAJOR ELEMENTS IN IGNEOUS ROCKS CLASSIFICATION OF IGNEOUS ROCKS – BASIS FASTEST COOLING RATE RESULTS

8. EXAMPLES OF APHANITIC ROCK, PHANERTIC ROCK 9. WHEN ROCKS MELT UNDER LOWER TEMPERATURE? 10.FACTORS THAT CONTROL MELTING POINT OF A MINERAL. 11. WHAT IS BOWEN’S REACTION SERIES?IT EXPLAINS WHAT?WHAT IS DISCONTINUOUS SERIES? 12. DIKE, SILL, BATHOLITHS, XENOLITHS 13. OCEANIC CRUST – BASALTS & GABBROS 14. WHAT TYPES OF MAGMA ASSOCIATED WITH WHAT BOUNDARIES