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Multiple Stressors in the Coastal Ocean

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Multiple Stressors in the Coastal Ocean PICES Annual Meeting, Oct. 16, 2013, Nanaimo, Canada Multiple stressors in the coastal ocean Minhan Dai (戴民汉) Collaborators: JW Liu, WP Jing, XH Guo, ZQ Yin 近海海洋环境科学国家重点实验室（厦门大学） State Key Laboratory of Marine Environmental Science (Xiamen University) Overview • Ocean Acidification (OA): Another CO2 problem has emerged– yet coastal ocean more complex • Coastal ecosystems under multiple forcings: temp rising + O2 decline+ acidification within a similar time frame • Need consider the hydrodynamics: e.g., Upwelling/Submarine Groundwater Discharge • OA observation system & multidisciplinary researches essential and consider the multiple stressors at a system level Outline • Coastal Ocean Acidification • Multiple stressors in the Coastal Ocean • Concluding Remarks Ocean Acidification: another CO2 problem: increase in [H+] or drawdown of pH When CO2 invades sea water: - • [HCO3 ]increases 2- • [CO3 ]decreases From PMEL • Ω decreases + + - pH = -log (H ) = -log gH{H } • a small part of HCO3 CaCO3 saturation state: formed dissociates into 2+ 2- + = [Ca ][CO3 ]/Ksp’, carbonates + H (“ocean a > 1 ~supersaturated acidification”) Calcification rate vs. arag in coral reef systems Shamberger et al. (2011) Why Coastal Ocean? • A unique physical- biogeochemical ecosystem links the land and the open ocean but vulnerable • Boundary processes across the land-margin and margin-ocean are key drivers • Characterized by complex circulations, abundant river/groundwater input, dynamic sediment boundary and high productivity: large gradients chemically and biologically An updated province –based global shelf air-sea CO2 flux: ~ 0.36 pg/yr Dai et al., GRL, 2013 Coastal ocean mitigates more CO2 than the open ocean pH dynamics in different marine systems Hofmann et al. (2011) High- Frequency Dynamics of Ocean pH: A Multi-Ecosystem Comparison. PLoS ONE 6(12): e28983. doi:10.1371/journal.pone.0028983 OA in coastal ocean more dramatic A NE Pacific Coastal Site (Tatoosh Island, 2000-2008) - Wootton et al., PNAS, 2008 OnOn--SiteSite ObservationObservation pH more variable in coastal systems Jiang et al., L&O, 2011 MEL-SMMC CO2-A Cases: main drivers of OA in coastal ocean – Anthropogenic CO2 – Upwellings of low pH waters – Respirations – Ground water Anthropogenic CO2-driven pH changes in the South China Basin Predicted anthropogenic The South China Sea CO2 induced pH decrease－ (Station SEATS, 1998-2009) 0.0019 yr-1 390 Surface pH decreasing: －0.002 yr-1 380 atm) ( 370 2 CO 360 p 350 8.06 8.05 SW 8.04 pH 3.68 8.03 3.64 arag 3.60 3.56 3.52 - Arthur Chen, MEBC-SCS Conference Abstract, 1998 2000 2002 2004 2006 2008 2010 2012 2010 Year http://mebc- -1 scs.marine.nsysu.edu.tw/images/Text/Abstract_Chen.pdf Air pCO2 2 atm yr At TAlk=2200 mol kg-1; Temp=29.0 oC; S=33.5; PO4=0.01 M; Si(OH)4=2 M Examples: OA in coastal ocean – Anthropogenic CO2 – Upwellings of low pH waters – Respirations – Ground water Aragonite Saturation Depth (arag = 1.0) in the Global Oceans - Feely et al., 2004 Coastal Upwelling System Western NP vs. Eastern NP Case I: Continental shelf off the Oregon-California border (Upwelling in the Eastern NP) Distribution of the depths of the undersaturated water (arag < 1.0; pH < 7.75) on the continental shelf of western North America. Due to the upwelling process, the corrosive water reaches all the way to the surface in the inshore waters near the Oregon-California border. - Feely et al., 2008 • Upwelling from depths of 150 to 200 m onto the shelf; • First observation of surface undersaturated waters with respect to aragonite (in open ocean surface waters until 2050); • ~30 mol kg-1 of anthropogenic CO2 lowered arag by ~0.2 units. - Feely et al., 2008 Case II: The Northern South China Sea (NSCS) Shelf (Upwelling in the Western NP) Field work-2008 summer Leg 1 ( Transects 1-7; Jun 30 - Jul 8) Leg 2 (Transects 5-2; Jul 9 - Jul 12) 2525 Mainland China 2424 S401c S401b N) S401a o 2323 Pearl River S201a estuary 2222 6 7 5 Latitude ( Latitude 2 4 1 3 2121 2020 112112 113113 114114 115115 116116 117117 118118 119119 120120 121121 122122 Longitude (oE) Leg 1 Surface Leg 2 24 24 31 Temp. (oC) Temp. (oC) 30 Upwelling Centers (UC): 23 23 29 Low Temperature 28 22 22 27 High DIC 26 Low arag 21 UC 1 21 UC 2 25 24 UC 2 > UC 1 20 20 23 114 115 116 117 118 119 120 114 115 116 117 118 119 120 24 24 DIC DIC 2040 -1 -1 1990 Surface arag values: 23 (mol kg ) 23 (mol kg ) 1940 1890 2.3 ~ 3.9 22 22 1840 Lowest 2.3 in UC 2 1790 21 21 1740 Oversaturation state 1690 20 20 1640 114 115 116 117 118 119 120 114 115 116 117 118 119 120 24 24 3.9 arag arag Upwelled waters were 3.7 23 23 3.5 transported 3.3 northward from the 22 22 3.1 position of UC 2 to the 2.9 position of UC 1 [Gan 21 21 2.7 2.5 et al., 2009]. 20 20 2.3 114 115 116 117 118 119 120 114 115 116 117 118 119 120 arag in the upwelling Leg 1 Leg 2 3.4 3.4 Transect 2 3.2 Transect 3 3.2 Lowest values in UC 1 and Transect 4 3.0 Transect 5 3.0 UC 2 were largely imprints 2.8 2.8 of upwelled subsurface 2.6 2.6 waters enriched with both arag arag 2.4 2.4 anthropogenic CO2 and Transect 2 2.2 Transect 4 2.2 respired CO2; 2.0 Stations S401a-c 2.0 (a) Transect 5 (c) 1.8 1.8 During the northward -80 -60 -40 -20 0 20 40 -80 -60 -40 -20 0 20 40 transport of the upwelled DIC (mol kg-1) DIC (mol kg-1) water, however, arag -80 -60 -40 -20 0 20 40 -80 -60 -40 -20 0 20 40 750 750 increased whereas fCO2 Transect 2 700 Transect 4 700 decreased with increasing 650 Stations S401a-c 650 Transect 5 DIC. The consistent 600 600 biological production atm) atm) ( 550 550 ( gradually consumed CO2 2 2 500 500 and raised [CO ], resulting CO CO 3 f f 450 Transect 2 450 in the increasing arag Transect 3 400 Transect 4 400 pattern in the upwelled (b) Transect 5 (d) 350 350 water. Behaviors of DIC, TAlk and Ca2+ in the upwelled water 2226 10100 y=(-0.18±0.06)x+(2577±129) r=0.89 ) 2224 -1 ) -1 10000 2222 y=(265.5±12.5)x+(948.3±428.7) mol kg 2220 r=0.99 ( mol kg 9900 2218 2+ 2216 y ± x ± /NCa =(-0.14 0.00) +(2482 2) 9800 NTAlk ( NTAlk r=1.00 2+ 2214 Ca (a) (b) 2212 9700 1940 1950 1960 1970 1980 1990 2000 34.0 34.1 34.2 34.3 34.4 NDIC (mol kg-1) Salinity • NDIC variations ~30 mol kg-1; NTAlk variations ~6 mol kg-1 • Slopes of NTAlk against NDIC were close to －0.16 OC metabolism: 106CO2+122H2O+16HNO3+H3PO4↔ (CH2O)106(NH3)16H3PO4+138O2, TAlk/DIC=－0.16 2+ - IC metabolsim: Ca +2HCO3 ↔CaCO3+CO2+H2O, TAlk/DIC=2 • Conservative behavior of Ca2+ No significant impact of the upwelling on the net community calcification! Summary for the NSCS upwelling • Upwelling delivered low arag waters onto the shelf, but arag values are still > 1.0; • Enhanced OC production during the upwelling further increased arag; • The patterns of arag are largely controlled by water circulation and biological activities at present; • Oversaturation for now. Context • Corrosive waters with < 1.0 may be possible on most of wide shelves including the NSCS shelf! • How the calcifying organisms, including many species of shellfish of economic importance to coastal regions, deal with this intermittent exposure of corrosive waters? China is the largest mariculture country, contributing to 68.81% of Seaweed Fish Crustacean 11% 5% 5% the total global yields (FAO, 2006); Shellfish is the most important composition. Shellfish 79% Production of shell fish in 2008 Composition of mariculture was ~ 10 MT yields of China in 2002 [Zhang et al., 2005] Aragonite Saturation Depth (arag = 1.0) in the Global Oceans - Feely et al., 2004 Source Water Depth ~150 m ~150 m Source Water pH ~7.95 < 7.75 Source Water arag ~1.9 < 1.0 Aragonite ~500 m in the 100-300 m in the Saturation Depth Western NP Eastern NP The contrasting scenarios between the two cases are related to the different “acidity” of source waters of upwelling. Examples: OA in coastal ocean – Anthropogenic CO2 – Upwellings of low pH waters – Respirations/nutrification – Ground water Respiration + Nitrification induced pH drawdown in the Pearl River Aerobic respiration (CH2O)106(NH3)16H3PO4 + 138 – O2 + 18 HCO3 124 CO2 + – 2– Pearl River Estuary 140 H2O + 16 NO3 + HPO4 Nitrification + – NH4 + 1.89 O2 + 1.98 HCO3 – 0.984 NO3 + 0.016 C5H7O2N +1.90 CO2 + 2.93 H2O Fig A from Zhang Cao Fig B from Guo et al., 2008, CSR DO saturation (%) Depth (m) Examples: OA in coastal ocean – Anthropogenic CO2 – Upwellings of low pH waters – Respirations – Ground water Acidification in Hainan Coral Reef Low pH in Sanya fringing reef system 8.2 ℃ 8.1 8.0 7.9 pH Sanya Coral Reef 7.8 pH Sanya Bay pH_total scale_@25 pH_total 7.7 2012- 2-6 2-7 2-8 2-9 2-10 2-11 2-12 2-13 2-14 Major processes related to OA in the coastal ocean Coastal ocean has large natural variability due to changes in physical and biological conditions and various anthropogenic impacts including: River Plume High TA Input pH ↑ Eutrophication CO2 ↓ pH ↑ OA pH ↓ Low TA Input pH ↓ Photosynthesis CO2 ↓ pH ↑ Respiration CO2 ↑ pH ↓ Upwelling + OM Respiration CO2 ↑ pH ↓ Coastal Upwelling High CO2 pH ↓ Basics about coastal OA • OA in coastal ocean? pH change in coastal ocean may be more complex, driven by anthropogenic CO2, riverine/groundwater input (eutrophication & respiration) and water circulation (upwelling of low pH/DO waters), and other biogeochemical reactions under low/no DO.
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