Initiation of precipitation via the ice phase Part I: Microphysical processes Karoline Diehl University of Mainz, Germany Institute of Atmospheric Physics Max-Planck Institute of Chemistry, Mainz COPS summer school July 2007 SFB 641: The tropospheric ice phase

Initiation of precipitation cloud droplet sizes: 2 to 100 µm rain drop sizes: 100 µm to 8 mm → cloud drops have to grow to larger sizes to fall out from the cloud → growth by diffusion of water vapor is not sufficient two main processes: 1.collision and coalescence (warm process) larger cloud drops collect smaller droplets

initiation of precipitation by a warm process cloud droplets < 50 µm radius too small to fall out coalescence (joining) formation of larger drops further collisions sampling of droplets with lower terminal velocities freely floated raindrop with 3 mm radius photo from the Mainz vertical wind tunnel

Initiation of precipitation cloud droplet sizes: 2 to 100 µm rain drop sizes: 100 µm to 8 mm → cloud drops have to grow to larger sizes to fall out from the cloud → growth by diffusion of water vapor is not sufficient two main processes: 1.collision and coalescence (warm process) larger cloud drops collect smaller droplets 2.ice particles (cold process) ice particles once formed grow at the expense of liquid drops

Initiation of precipitation via the ice phase major fraction of precipitation is initialized by a cold process troposphere: mostly mixed phase clouds → coexistence of super-cooled liquid drops and ice particles ▪ super-cooled liquid drops down to -40°C ▪ incidence of ice around -4°C

Incidence of ice in clouds from: Pruppacher and Klett, 1997

Initiation of precipitation via the ice phase ice nuclei formation of ice growth of ice particles

Definition of ice nuclei ice nuclei are aerosol particles which trigger the transition from vapor to ice phase requirements: *insolubility *size > 0.1 µm *ice active sites on the surface *crystallographic shape similar to ice atmospheric concentrations of ice nuclei: < 10 per liter well-known types of atmospheric ice nuclei: mineral dust, soot particles, biological particles

Formation of ice *sublimation of water vapor on ice nuclei *condensation of water vapor on ice nuclei, followed by freezing *freezing of super-cooled drops 1. homogeneously without ice nuclei 2. heterogeneously with ice nuclei a) ice nuclei suspended in drops b) ice nuclei collide with drops

Formation of ice: Deposition freezing sublimation of water vapor on ice nuclei → deposition freezing requirements: dry ice nucleus super-saturation with respect to ice critical temperature to initiate ice nucleation result: ice crystals in various habits, dependant on 1. temperature 2. super-saturation

Basic habit of ice crystals crystallographic: hexagonal prism two basal planes of type (0001) six prism planes pf type (1010)

from: Furukawa, 1997

crystallographic: hexagonal prism (sixfold symmetric) two basal planes of type (0001) six prism plates pf type (1010) habit of crystals determined by preferential axis during growth: major axis c minor axes a 1, a 2, a 3 Basic habit of ice crystals

crystallographic: hexagonal prism (sixfold symmetric) two basal planes of type (0001) six prism plates pf type (1010) habit of crystals determined by preferential axis during growth: major axis c minor axes a 1, a 2, a 3 cyclic change of preferred axis with decreasing temperature: plate column -4°C -9°C -22°C with increasing super-saturation: habit of ice crystals changes but not preferential axis Basic habit of ice crystals

from: Kobayashi and Kuroda, 1987 Photos of elemental ice crystals

Classification of ice crystals from: Pruppacher and Klett, 1997 Magono-Lee classification table of natural ice crystals – some examples left panel: elementary habits right panel: change of environmental conditions during growth → crystal continue growth according to new conditions → appear as combinations of different shapes but: crystallographic point of view: still single crystals with c and a axes throughout the crystal

Formation of ice: Condensation freezing condensation of water vapor on ice nuclei, followed by freezing of the drop → condensation freezing requirements: dry ice nucleus which is suited as condensation nucleus super-saturation with respect to water critical temperature to initiate ice nucleation result: frozen drop

Formation of ice: Condensation freezing Experiments at the Institute of Atmospheric Research, Mainz: super-saturation chamber, temperature < 0°C scattering of particles into the chamber sampling of ice particles on formvar plates 1. biological particles (pollen) drop diameters between 110 and 170 µm from: Diehl et al., 2001

Formation of ice: Condensation freezing Experiments at the Institute of Atmospheric Research, Mainz: 2. soot particles from a kerosene burner ice crystal diameters between 40 and 100 µm from: Diehl and Mitra, 1998

Formation of ice: Deposition and condensation freezing as function of temperature and super-saturation Threshold curves of various ice nuclei for deposition and condensation freezing from: Schaller and Fukuta, 1979

Formation of ice: Freezing of super-cooled drops Homogeneous freezing dependant on temperature and drop volume from: Mason, 1971 Homogeneous freezing relationship between temperature and drop diameter for freezing of super-cooled drops

Formation of ice: Freezing of super-cooled drops Heterogeneous freezing: Immersion mode dependant on temperature, drop volume, type of ice nuclei efficiency of ice nuclei expressed by median freezing temperature T m, i.e. the temperature where 50% of an observed drop population freeze → determined in laboratory experiments examples for different ice nuclei, a ≈ 300 µm T m = -33° C for pure drops (Mason, 1971) T m = -28° C for soot particles (Diehl and Mitra, 1998) T m = -23° C for kaolinite (Pitter and Pruppacher, 1973) T m = -19° C for montmorillonite (Pitter and Pruppacher, 1973) T m = -9° C for leaf litter (Diehl et al., 2001) T m = -7° C for bacteria (Levin and Yankofsky, 1983)

Formation of ice: Freezing of super-cooled drops Heterogeneous freezing: Immersion mode Results from experiments at the Mainz vertical wind tunnel soot particles from kerosene burner (Diehl and Mitra, 1998) pollen (Diehl et al., 2002, v. Blohn et al., 2005) leaf litter (Diehl et al., 2001)

Formation of ice: Freezing of super-cooled drops Heterogeneous freezing: Immersion mode dependant on temperature, drop volume, type of ice nuclei examples for different drop radii, ice nuclei are montmorillonite T m = -24° C for a = 50 µm (Hoffer, 1961) T m = -19° C for a = 350 µm (Pitter and Pruppacher, 1973) median freezing temperature ~ ln (drop volume)

Formation of ice: Freezing of super-cooled drops Heterogeneous freezing: Contact mode dependant on temperature, type of ice nuclei efficiency of ice nuclei expressed by median freezing temperature T m examples for different ice nuclei T m = -18° C for soot particles (Gorbunov et al., 2001) T m = -12° C for kaolinite (Pitter and Pruppacher, 1973) T m = -10° C for leaf litter (Diehl et al., 2001) T m = -8° C for montmorillonite (Pitter and Pruppacher, 1973) T m = -5° C for bacteria (Levin and Yankofsky, 1983)

Formation of ice: Freezing of super-cooled drops Heterogeneous freezing: Contact mode Results from experiments at the Mainz vertical wind tunnel pollen (Diehl et al., 2002, v. Blohn et al., 2005) contact freezing versus immersion freezing

Formation of ice: Freezing of super-cooled drops Heterogeneous freezing: Contact mode → seems to be a very efficient process, but: it is restricted by the collision efficiency between drops and aerosol particles, which is dependant on: ▪ Brown diffusion ▪ thermo-phoretic and diffusio-phoretic forces ▪ inertia effects ▪ electrical forces collision kernel dependant on terminal velocities and cross sections of colliding partners:

Maximum ice particle concentration in various cloud types As – altostratus, S – stratus, Sc – stratocumulus, Cu – cumulus, C(S) – cumulus with stratified tops from: Pruppacher and Klett, 1997 ice particle concentration is not a sensitive function of temperature → fast glaciation discrepancy between concentrations of ice nuclei and ice particles → ice multiplication ▪ mechanical fracturing of fragile ice crystals ▪ splintering during drop freezing or during riming

Growth of ice particles deposition of water vapor riming agglomeration

Growth of ice particles 1. Deposition of water vapor p–T phase diagram of bulk water from: Pruppacher and Klett, 1997 at temperatures below 0°C: saturation vapor pressure above ice lower than the saturation vapor pressure above super-cooled water maximum difference at -12°C

Growth of ice particles 1. Deposition of water vapor at temperatures between 0 and -30°C: the saturation vapor pressure above ice is lower than the saturation vapor pressure above super-cooled water no equilibrium between super-cooled water drops and ice particles ice particles grow at the expense of liquid drops → Bergeron-Findeisen process

Growth of ice particles 2. Riming deposition of super-cooled liquid droplets on frozen drops or ice crystals → collision process → dependant on collision partners

Growth of ice particles 2. Riming relationship between onset of riming and radius of ice crystals open columns: unrimed crystals solid columns: rimed crystals from: Pruppacher and Klett, 1997 increasing complexity of ice crystal → increasing size of rimed ice crystals

Growth of ice particles 2. Riming observed size distributions of cloud droplets deposited on planar ice crystals from: Pruppacher and Klett, 1997 minimum droplet size: 10 µm maximum droplet size: 80 µm increasing size of ice crystal → broader droplet size spectrum

Growth of ice particles 2. Riming deposition of super-cooled liquid droplets on frozen drops or ice crystals →rimed ice crystals original habit still visible

Growth of ice particles 2. Riming Rimed planar ice crystals of 2 to 3 mm diameter, rimed column ice crystal of 1.5 mm length from: Pruppacher and Klett, 1997

Growth of ice particles 2. Riming deposition of super-cooled liquid droplets on frozen drops or ice crystals →rimed ice crystals original habit still visible →graupel original habit no more visible conical graupel or lump graupel

Growth of ice particles 2. Riming conical and lump graupel from: Pruppacher and Klett, 1997 growth of graupel 1.deposition of super- cooled droplets mainly at the lower side → conical graupel 2.balance point changing → tumbling → lump graupel

Growth of ice particles 2. Riming deposition of super-cooled liquid droplets on frozen drops or ice crystals →rimed ice crystals original habit still visible →graupel original habit not visible conical graupel or lump graupel →hailstones diameter > 5 mm in extreme cases: sizes up to 10 cm

Growth of ice particles 2. Riming thin section of hailstone diameter 4 cm from: Pruppacher and Klett, 1997 ▪ visible germ in the hailstone center → frozen drop or graupel ▪ onion-like structure: clear and opaque layers clear layers: temperature slightly below 0°C, much super-cooled water → fast freezing hinders crystallization → solidified melt opaque layers: low temperatures, little super-cooled water → slow freezing, crystallization, inclusion of air bubbles

Growth of ice particles 3. Agglomeration agglomeration of ice crystals → snow flake *crystal shape complex habit with branches favored *temperature quasi-liquid layer at ice surface 1 × µm at -1°C 1 × µm at -20°C maximum dimensions: 0.5 to 12 mm

hydrometeorssizeterminal velocity cloud droplets< 100 µm< 0.25 m/s rain drops100 µm – 8 mm0.25 m/s – 4 m/s ice crystals< 1.5 mm< 0.6 m/s snow flakes1 mm – 12 mm0.5 m/s – 1.5 m/s graupel0.5 mm – 4 mm0.75 m/s – 3 m/s hailstones5 mm – 8 cm5 m/s – 50 m/s Terminal velocities of hydrometeors

Initiation of precipitation via the ice phase mixed phase clouds: *ice particles are present at temperatures as high as -4°C *ice particles grow mainly at the expense of liquid drops → fast glaciation of clouds → ice particles reach large terminal velocities *efficient formation of precipitation-sized ice particles

Initiation of precipitation via the ice phase mixed phase clouds: *ice particles are present at temperatures as high as -4°C *ice particles grow mainly at the expense of liquid drops → fast glaciation of clouds → ice particles reach large terminal velocities *efficient formation of precipitation-sized ice particles highly important for special cases: suppression of warm rain examples: biomass burning, strong pollution small aerosol particles → formation of small drops reduced formation of precipitation sized drops via collision and coalescence

Initiation of precipitation by cold processes cloud droplets frozen drop riming water vapor graupel hailstone ice nuclei water vapor ice crystal growing by riming cold precipitation melting warm precipitation 0°C snow flake agglomeration rimed crystal