OCN520 Fall 2009 Mid-Term #2 Review Since Mid-Term #1 Ocean Carbonate Distributions Ocean Acidification Stable Isotopes Radioactive Isotopes Nutrients.

Slides:

Advertisements

Similar presentations

Principles of Mass Balance

Advertisements

Lecture 5 Stable Isotopes

1 Carbon Cycle 9 Carbon cycle is critically important to climate because it regulates the amount of CO 2 and CH 4 in the atmosphere. Carbon, like water,

Carbonate System and pH

Triple Oxygen Isotopes 11/1/10

Dissolution of calcite in sediments -- metabolic dissolution.

Lecture 19 The Ocean Nitrogen Cycle Sinks/Sources Sink - Denitrification Reactions Distributions Source - Nitrogen Fixation Reactions Distributions The.

Lecture 2 - Major Ions in Sea Water Why do we care about the major ions? What is the composition of seawater? What defines Major Ions? What are their concentrations?

GEOF236 CHEMICAL OCEANOGRAPHY (HØST 2012) Christoph Heinze University of Bergen, Geophysical Institute and Bjerknes Centre for Climate Research Prof. in.

OXYGEN ISOTOPES B.C. Schreiber U. Washington Dept. Earth & Space Science To be used only for scholarly purposes, consistent with “fair use” as prescribed.

The Carbon Cycle The carbon cycle describes the exchange of carbon atoms between various reservoirs within the earth system. The carbon cycle is a geochemical.

Lecture 10: Ocean Carbonate Chemistry: Ocean Distributions Controls on Distributions What is the distribution of CO 2 added to the ocean? See Section 4.4.

Coastal Upwelling Equatorward winds along a coastline lead to offshore Ekman transport Mass conservation requires these waters replaced by cold, denser.

Methane and Nitrous Oxide distributions in natural waters around Taiwan Hsiao-Chun Tseng, Chen-Tung Arthur Chen, Ting-Yu Chen ＊, Hung-Ling Chen,Meng-Chia.

Lecture 16 Oxygen distributions and ocean ventilation Thermocline Ventilation and Deep Water Formation Oxygen Utilization rates.

Lecture 15 natural sulfur, acid rain Rainout We mentioned a few of things that may rainout: 1.CH 3 OOH (CH 4 oxidation, low NO x ) 2.H 2 O 2 (CO oxidation,

Lecture 11 Stable Isotopes

Principles of Mass Balance

Lecture 13 Tracers for Gas Exchange Examples for gas exchange using: 222 Rn 14 C E&H Sections 5.2 and 10.2.

Lecture 10: Ocean Carbonate Chemistry: Ocean Distributions Controls on Distributions What is the distribution of CO 2 added to the ocean? See Section 4.4.

The Anthropogenic Ocean Carbon Sink Alan Cohn March 29, 2006

1 River Discharge Stream Animation. 2 Surface Currents.

Lecture 18 The Ocean Nitrogen Cycle Denitrification Reactions Distributions Nitrogen Fixation Reactions Distributions.

Carbonates Madelon van den Hooven

Parasitism and Symbiosis: isotope effects in mistletoe and foraminifera 1998)

Lecture 12 Primary Production – Nutrient Stoichiometry Topics Stoichiometry Biolimiting Elements.

OS13B Modeling the Distribution and  15 N of Nitrogen Gas and Nitrogen Species in the Black Sea S. K. Konovalov 1, C. A. Fuchsman 2 and J.W. Murray.

Properties of Gas in Water Oxygen Sources and Sinks Oxygen Distribution (space & time) Measuring Dissolved Oxygen Measuring 1º Production and Respiration.

Chemical and Physical Structures of the Ocean. Oceans and Temperature Ocean surface temperature strongly correlates with latitude because insolation,

GEOLOGIC CARBON CYCLE Textbook chapter 5, 6 & 14 Global carbon cycle Long-term stability and feedback.

Extra Credit #3 n May 4 (Monday), 7:30pm Byrne Lecture Dr. Eddie Bernard, NOAA “Tsunamis” Austin Auditorium LaSells Stewart center 1-page reaction paper.

Class The Oceans More on the chemistry of the Oceans... DISSOLVED GASES IN SEA WATER Solubility of atmospheric gases Solubility of atmospheric gases.

The Other Carbon Dioxide Problem Ocean acidification is the term given to the chemical changes in the ocean as a result of carbon dioxide emissions.

Ocean circulation, carbon cycle and oxygen cycle Anand Gnanadesikan FESD Meeting January 13, 2012.

Marine Geochemistry 2 Reference: Schulz and Zabel Marine Geochemistry Springer, New York pp. ISBN X.

Seawater Seawater is a solution of about 96.5% water and 3.5% dissolved salts. The most abundant salt in seawater is sodium chloride (NaCl). Most elements.

What can O 2 tell us about the climate change in the oceans? Taka Ito School of Earth and Atmospheric Sciences Georgia Institute.

Iron and Biogeochemical Cycles

CO 2 and Climate Change. Lisiecki & Raymo,

PH and Chemical Equilibrium. Acid-base balance Water can separate to form ions H + and OH - In fresh water, these ions are equally balanced An imbalance.

1 Basic Ocean Chemistry AOSC 620 Why do we care? Source of much food. Sink for much CO 2 and acids. Biodiversity. Great store and transport of heat. Source.

Announcements in class 2/5/07 Movie Wed. Don’t miss it! Material will be on the exam. Only one showing. Problem Set 4 is posted online. Print it out yourself.

Interpreting the sedimentary record

Nutrients & Tracers Nutrients & Tracers

Lecture 10: Ocean Carbonate Chemistry: Ocean Distributions

Paleoceanography. The Start ► HMS Challenger 1700s—info about sed distribution ► Piston corer (1940’s) showed CaCO3 ► Ocean environment varied ► Challenged.

Oceans & Anthropogenic CO 2 V.Y. Chow EPS 131.  CO 2 exchange across sea surfaces in the oceans  Measurement methods of anthropogenic CO 2  Distributions.

Pore water profiles of reactants or products can be a sensitive way to estimate OM decomposition rates. Oxic respiration (assuming Redfield ratio): (CH.

The Carbon Cycle. Carbon Dioxide and Carbonate system Why is it important? 1. Regulates temperature of the planet 2. Important for life in the ocean 3.

Carbonate Solubility Solubility Dissolution mechanisms Dissolution rate expressions Saturation state in the ocean T, P, and CO 2 release In situ [CO 3.

Isotopic insights into the benthic N cycle, and its impact on the global marine N cycle. Start with a review of stable isotope behavior in general. Wind.

Chemical & Physical Properties of SeaWater

Dissolution of calcite in sediments -- metabolic dissolution.

Carbonate System and pH Why study the carbonate system? Why study the carbonate system? Involves carbonic acid – an example of an acid-base reaction Involves.

Unit. 2 Mr. Lara Marine Science Class

Food web and microbial loop Eutrophic vs. Oligotrophic food webs

Chapter 8—Part 2 Basics of ocean structure The Inorganic Carbon Cycle/

Projected changes to the tropical Pacific Ocean

Projected changes to the tropical Pacific Ocean

222Rn, oxygen, nutrients (nitrate, ammonia, phosphate)

Carbon cycle theme The Earth’s carbon cycle has a stabilizing mechanism against sudden addition of CO2 to the atmosphere About 50% of carbon emission is.

The Oceanic Sink Uptake in the mixed layer

Week 12: Nutrient and carbon cycling

Iron and Biogeochemical Cycles

Week 12: Nutrient and carbon cycling

Food web and microbial loop Eutrophic vs. Oligotrophic food webs

Projected changes to the tropical Pacific Ocean

Geologic carbon cycle Textbook chapter 5, 6 & 14 Global carbon cycle

Projected changes to the tropical Pacific Ocean

Presentation transcript:

OCN520 Fall 2009 Mid-Term #2 Review Since Mid-Term #1 Ocean Carbonate Distributions Ocean Acidification Stable Isotopes Radioactive Isotopes Nutrients and Production POC Export and Respiration O2: Ventilation versus Respiration

Sarmiento and Gruber (2002) Sinks for Anthropogenic Carbon Physics Today August

Ocean Distributions – versus depth, versus ocean Atlantic Pacific Points: 1. Uniform surface concentrations 2. Surface depletion - Deep enrichment 3. DIC < Alk  DIC >  Alk See Key et al (2004) GBC Q?

The main features are: 1. uniform surface values 2. increase with depth 3. Deep ocean values increase from the Atlantic to the Pacific 4. DIC < Alk  DIC >  Alk 5. Profile of pH is similar in shape to O Profile of P CO2 (not shown) mirrors O 2. Ocean Distributions of, DIC, Alk, O 2 and PO 4 versus Depth and Ocean

Paleo Nutrient Distributions Boyle and Keigwin (1982) Science Data in benthic forams – North Atlantic

Controls on Ocean Distributions A) Photosynthesis/Respiration Organic matter (approximated as CH 2 O for this example) is produced and consumed as follows: CH 2 O + O 2  CO 2 + H 2 O Then: CO 2 + H 2 O  H 2 CO 3 * H 2 CO 3 *  H + + HCO 3 - HCO 3 -  H + + CO 3 2- As CO 2 is produced during respiration we should observe: pH  DIC  Alk  P CO2  The trends will be the opposite for photosynthesis. B) CaCO 3 dissolution/precipitation CaCO 3 (s)  Ca 2+ + CO 3 2- Also written as: CaCO 3 (s) + CO 2 + H 2 O  Ca HCO 3 - As CaCO 3 (s) dissolves, CO 3 2- is added to solution. We should observe: pH  DIC  Alk  P CO2 

Emerson and Hedges Color Plate  DIC/  Alk ≈ 1.5/1 Work Backwards  Alk /  DIC ≈ 0.66 = 2/3 = 2 mol Org C / 1 mol CaCO 3

 18 O of planktonic and benthic foraminifera from piston core V (160ºE 1ºN) Planktonic and Benthic differ due to differences in water temperature where they grow. Planktonic forams measure sea surface T Benthic forams measure benthic T Example: Estimation of temperature in ancient ocean environments CaCO 3 (s) + H 2 18 O  CaC 18 OO 2 + H 2 O The exchange of 18 O between CaCO 3 and H 2 O The distribution is Temperature dependent Assumptions: 1. Organism ppted CaCO 3 in isotopic equilibrium with dissolved CO The δ 18 O of the original water is known 3. The δ 18 O of the shell has remained unchanged last glacialHolocene last interglacial

δ 13 C in different reservoirs E & H Fig. 5.6

Distillation of meteoric water – large kinetic fractionation occurs between ocean and vapor. Then rain forming in clouds is in equilibrium with vapor and is heavier that the vapor. Vapor becomes progressively lighter.  D and  18 O get lower with distance from source. Water evaporation is a kinetic effect. Vapor is lighter than liquid. At 20ºC the difference is 9‰ (see Raleigh plot). The BP of H 2 18 O is higher than for H 2 16 O Air masses transported to higher latitudes where it is cooler. water lost due to rain raindrops are rich in 18 O relative to cloud. Cloud gets lighter

Secular equilibrium  1/2 daughter = 0.8 hr  1/2 parent =  time (hr) Activity (log scale) daughter  1/2 parent ! Daughter grows in with half life of the daughter!

222 Rn Example Profile from North Atlantic 226 Ra 222 Rn Does Secular Equilibrium Apply? t 1/2 222Rn << t 1/2 226Ra (3.8 d) (1600 yrs) YES! A 226Ra = A 222Rn Why is 222 Rn activity less than 226 Ra?

Coale & Bruland 1987 Particle and 234 Th Export Vertical zonation of 234 Th removal

Annual Mean Surface Nitrate

The Redfield or "RKR" Equation (A Model) The mean elemental ratio of marine organic particles is given as: P : N : C = 1 : 16 : 106 The average ocean photosynthesis (forward) and aerobic ( O 2 ) respiration (reverse) is written as: 106 CO HNO 3 + H 3 PO H 2 O + trace elements (e.g. Fe) light (h )  ( C 106 H 263 O 110 N 16 P ) O 2 or (CH 2 O) 106 (NH 3 ) 16 (H 3 PO 4 ) Algal Protoplasm The actual chemical species assimilated during this reaction are: HCO 3 - NO 3 - PO 4 3- NO 2 - NH 4 +

Food Web Cartoon PON DON Euphotic Zone (~100m) At steady state: New NO 3 = O 2 flux to atm = PON (and DON) export Follow the N! Follow the C! Follow the O 2 ! Fe plays a role!

Surface fingerprints: ventilation thermocline Mixed layer Atm. thermocline Mixed layer Atm. Decrease ventilation Air-sea O 2 flux ΔAOU subtropics time outcrop An increase in AOU due to decreased ventilation will cause changes in air-sea fluxes of both O 2 and CO 2 coincident with the ventilation change…

Surface fingerprints: export thermocline Mixed layer Atm. thermocline Mixed layer Atm. Increase export flux Export flux Air-sea O 2 flux ΔAOU outcrop time subtropics Similar AOU anomalies may be caused by increased export flux, with very different signatures of O 2 /CO 2 gas exchange.